A lithostratigraphical framework for the Carboniferous successions of

A lithostratigraphical framework 

for the Carboniferous successions 

of northern Great Britain 

(onshore) 

Research Report RR/10/07

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Keywords 

Carboniferous, northern 

Britain, lithostratigraphy, 

chronostratigraphy, biostratigraphy. 

Front cover 

view of Kae Heughs, Garleton 

Hills, east lothian. showing 

Chadian to Arundian lavas and 

tuffs of the Garleton Hills volcanic 

Formation (strathclyde Group) 

exposed in a prominent scarp 

(p001032). 

Bibliographical reference 

Dean, M T, Browne, M a e, 

waTers, C n, and Powell, J H. 

2011. A lithostratigraphical 

framework for the Carboniferous 

successions of northern Great 

Britain (onshore). British 

Geological Survey Research 

Report, RR/10/07. 174pp. 

isBN 978 0 85272 665 5 

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BRiTisH GeoloGiCAl suRvey 

ReseARCH RepoRT RR/10/07 

A lithostratigraphical framework 

for the Carboniferous successions 

of northern Great Britain 

(onshore) 

m T dean, m A e Browne, C N waters and J H powell 

Contributors: m C Akhurst, s d G Campbell, R A Hughes, e w Johnson, 

N s Jones, d J d lawrence, m mcCormac, A A mcmillan, d millward, 

R A smith, d stephenson and B young 

maps and diagrams in this book 

use topography based on ordnance 

survey mapping. 

© NERC 2011. All rights reserved Keyworth, Nottingham British Geological survey 2011

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Foreword 

This report is the published product of a study by the 

British Geological survey (BGs) stratigraphical Framework 

Committee (sFC) of the Carboniferous rocks of northern 

Great Britain. The report provides a summary of a lithostratigraphical 

scheme proposed by the sFC that aims to rationalise 

group and formation nomenclature for the Carboniferous 

rocks of the entire onshore area of northern Great Britain. 

The study draws upon a published overview report for the 

Carboniferous of Great Britain (waters, et al., 2007), which 

identifies a group framework based upon the identification 

of nine major lithofacies associations across Britain. This 

framework report provides further, more-detailed descriptions 

of group and formation nomenclature, specifically 

for the onshore area of northern Great Britain (essentially 

north of the Craven Fault system) including the midland 

iii 

valley of scotland, southern scotland, northern england 

and the isle of man. it provides criteria for rationalisation 

of existing nomenclature where necessary. existing names 

are used wherever appropriate, although where formation 

names have not previously existed the report proposes a 

new nomenclature and provides a full description. This 

framework report is produced in conjunction with a framework 

report for onshore southern Great Britain (see waters 

et al., 2009). 

BGs stratigraphical Framework reports are published 

in collaboration with the stratigraphy Commission of the 

Geological society of london through the BGs internet 

website www.bgs.ac.uk where they are available as free 

downloads. Reports are peer-reviewed via the Geological 

society of london’s stratigraphy Commission. 

British Geological Survey 


Acknowledgments 

This report is the result of much discussion and lively 

debate within the BGs regarding the formulation of a 

comprehensive hierarchical lithostratigraphical scheme 

for the onshore successions of Great Britain. in 1999 dr 

peter Allen (Assistant director, BGs) requested that the 

chairmen of the established stratigraphical Framework 

Committee, mike Browne (midland valley of scotland), 

Nick Riley (Namurian of the pennines) and Brian young 

(Carboniferous of the scottish Borders and northern 

england) investigate the possibility of producing a uK 

wide subdivision of dinantian and Namurian lithostratigraphy 

at group level. Following a meeting held on 11 June 

1999 a top-down approach, defining groups by broad 

lithological facies was proposed, and schematic correlation 

figures were generated to indicate the distribution 

of these main lithofacies types. This proposal forms 

the basis of the subsequent scheme published within an 

overview report for the entire uK onshore (waters et al., 


Research Report RR/10/07 

iv 

2007). The subsequent task, detailed in this report, was to 

complete a comprehensive lithostratigraphical description 

of northern Great Britain. The authors of and contributors 

to this report include those who produced the lexicon 

entries for many of the units described. However, it is 

particularly important to acknowledge the contribution of 

d stephenson in the compilation of section 4.3.3 on the 

Clyde plateau volcanic Formation. The authors of the 

report gratefully acknowledge the contribution of many 

others in BGs who have offered constructive advice, 

especially d J lowe in his role as lexicon manager. The 

comments of the BGs stratigraphy Committee (Chaired 

by J H powell) and the external reviewers, dr ian 

somerville (university College dublin) and dr Gilbert 

Kelling (university of Keele), are also acknowledged. 

Joanna Thomas is thanked for editing the report and 

louise wilson, stuart Horsburgh and paul lappage are 

thanked for the drafting of the figures.

Contents 

Foreword iii 

Acknowledgements iv 

Summary vii 

1 Introduction 1 

1.1 Tectonic setting 1 

1.2 palaeogeography 1 

2 Correlation and biostratigraphical framework 5 

2.1 Chronostratigraphy 5 

2.2 Biostratigraphy 5 

3 Lithostratigraphical framework 11 

3.1 Group framework 11 

3.2 Formation framework 13 

4 Carboniferous rocks of Scotland north of the 

Southern Upland Fault 14 

4.1 midland valley of scotland 14 

4.2 inverclyde Group 14 

isle of Arran 20 

isle of Bute 20 

Cumbrae isles 21 

south of the River Clyde 21 

North of the River Clyde 22 

4.3 strathclyde Group 22 

west central scotland 23 

Renfrewshire Hills 24 

Beith – Barrhead Hills 27 

dunlop – eaglesham Block 29 

Kilpatrick Hills 32 

Campsie Block 35 

Fintry–Touch Block 47 

Ayr 53 

Fife 55 

west lothian and edinburgh 57 

east lothian 60 

4.4 Bathgate Group 62 

4.5 Clackmannan Group 64 

4.6 scottish Coal measures Group 69 

5 Carboniferous rocks of the Southern Uplands of 

Scotland 72 

5.1 The sanquhar and Thornhill basins 72 

5.2 yoredale Group 72 

5.3 Clackmannan Group 72 

sanquhar Basin 72 

Thornhill Basin 73 

5.4 scottish Coal measures Group 74 

6 Carboniferous rocks of the Northern England 

Province 77 

6.1 introduction 77 

6.2 ungrouped formations of continental and peritidal 

facies in the Craven Basin 77 

6.3 inverclyde Group 78 

6.4 Ravenstonedale Group 83 

stainmore Trough 84 

Askrigg Block 89 

isle of man 89 

6.5 Border Group 90 

6.6 Great scar limestone Group 95 

Alston Block 96 

v 

stainmore Trough and Ravenstonedale 97 

Askrigg Block 101 

Askrigg Block–Craven Basin Transition Zone 103 

south Cumbria 106 

North and west Cumbria 109 

isle of man 110 

6.7 yoredale Group 113 

6.8 Craven Group 128 

6.9 millstone Grit Group 132 

6.10 pennine Coal measures Group 137 

6.11 warwickshire Group 141 

7 References 145 

Appendix 1 Alphabetical listing of lithostratigraphical 

units 154 

Appendix 2 BGs lexicon of Named Rock units computer 

codes 159 

Appendix 3 Alphabetical listing of obsolete 

lithostratigraphical terms 161 

FIGURES 

1 principal structural features of the northern British 

isles 3 

2 palaeogeographical reconstructions for the 

Carboniferous of the British isles 4 

3 extent of Carboniferous rocks of onshore northern 

Great Britain 7 

4 schematic graphic log summarising the nine main 

lithofacies 12 

5 lithostratigraphical nomenclature for the midland 

valley of scotland 15 

6 Generalised vertical sections and correlation for 

Carboniferous strata in scotland 16 

7 lithostratigraphical nomenclature for the Northern 

england region 79 


Carboniferous strata in the isle of man, Canonbie and 

Northumberland 80 


Carboniferous strata in Cumbria, Alston, stainmore, 

Askrigg and the ingleton Coalfield 85 

10 solway Basin. Representative sections for 

Carboniferous strata at orroland and wall Hill, 

Kirkbean and langholm 87 

11 solway Basin. Representative sections for 

Carboniferous strata at Brampton, Bewcastle and 

Brampton (North) and Bellingham 93 

12 Northumberland Trough. Generalised vertical sections 

for Carboniferous strata at Berwick-upon-Tweed, Ford, 

Holy island and Alnwick 118 

13 Northumberland Trough. Generalised vertical sections 

for Carboniferous strata at elsdon, Rothbury and 

morpeth 119 

14 Cumbria. Representative sections for Carboniferous 

strata at west, North and east Cumbria 120 

15 Askrigg Block. Representative sections for 

Carboniferous strata at various localities 122 



TABLES 

1 Chronostratigraphical framework for the Carboniferous 

system of Great Britain 6 

2 Tournaisian and visean biostratigraphical zonations 8 

3 summary of the chronostratigraphical units of 

the Namurian and the main biozones for the most 

important fossil groups 9 

4 westphalian chronostratigraphy and biostratigraphical 

zonations 10 



vi

summary 

The stratigraphy Committee of the British Geological survey 

(BGs) is undertaking a review of stratigraphical classification 

for all parts of Great Britain. several stratigraphical 

Framework Committees (sFC) have been established 

to review problematical issues for various parts of the 

stratigraphical column. each sFC has the following terms of 

reference: 

• to review the lithostratigraphical nomenclature of 

designated stratigraphical successions for a given 

region, identifying problems in classification and 

correlation 

• to propose a lithostratigraphical framework down to 

formation level 

• to organise peer review of the scheme 

• to present the results in a document suitable for 

publication 

• to ensure that full definitions of the lithostratigraphical 

units are held in the web-accessible BGs lexicon 

of Named Rock units for the areas of responsibility 

covered by the sFC. 

The economic importance of strata of Carboniferous age 

has resulted in over 200 years of research attempting to 

classify them. much of this work occurred long before guidance 

was available for best practice in naming lithostratigraphical 

units. Consequently, a haphazard approach to the 

establishment of the hierarchy of units has resulted. From 

an early, relatively simple framework, subsequent surveys 

and publications have greatly added to the complexity of the 

nomenclature. often, this reflected the localised nature of 

research with a tendency to identify numerous local names 

for essentially the same unit. Also, end Carboniferous and 

subsequent tectonic events have resulted in the isolation by 

faulting or erosion of laterally contiguous deposits often 

resulting in a plethora of local names. This complexity 

in nomenclature has, to an extent, hindered the regional 

understanding of the Carboniferous successions throughout 

Great Britain. 

Two committees have reported on the Carboniferous 

succession of the midland valley of scotland (Browne et 

al., 1999) and the westphalian to early permian red-bed 

successions of the pennine Basin (powell et al., 2000) 

vii 

respectively. Further committees were established to review 

the Carboniferous successions of the scottish Borders and 

the Namurian successions of the pennine Basin. in 2000, 

these committees were subsumed into a single committee, 

which reviewed the entire Carboniferous successions 

throughout Great Britain. 

This report summarises the sFC lithostratigraphical 

scheme for onshore Carboniferous successions of northern 

Great Britain. A further report summarises the scheme 

employed in southern Great Britain (see waters et al., 

2009). 

The first part of this report summarises the structural 

and palaeogeographical setting of northern Great Britain 

throughout the Carboniferous period. 

The second part describes the key techniques of correlation 

of successions, principally biostratigraphy. 

The third part indicates the principle for the development 

of the new lithostratigraphical scheme. This demonstrates 

how the group hierarchy has been linked to major 

lithofacies and the procedures for rationalising existing 

nomenclature. 

The fourth and largest part of the report provides a 

full description of the group and formation framework 

for each of three regions; scotland north of the southern 

upland Fault, southern scotland, and the Northern england 

province (including the isle of man). each entry includes 

the rank of the nomenclature, and a description of its origin 

and history and key references, principal lithologies, 

environment of deposition, stratotypes, lower and upper 

boundaries, thickness, geographical extent, age range and 

any subdivisions to member level. The members themselves 

are similarly fully described. 

An appendix (Appendix 1) provides an alphabetical 

listing of each supergroup, group, formation and member 

respectively, and shows the heirarchical relationship 

between the lithostratigraphical units. it also provides computer 

codes from the BGs lexicon of Named Rock units 

where these have been allocated. Appendix 2 gives the 

BGs lexicon of Named Rock units computer codes for the 

lithostratigraphical beds shown in Figures 6 and 8–15 and 

Appendix 3 lists all the obsolete lithostratigraphical terms 

mentioned in the text and provides the units they are now 

equivalent to or included within. 





viii

1 introduction 

The Carboniferous strata of Great Britain comprise a wide 

range of facies representing a large variety of depositional 

environments. This in part reflects a northward drift 

of Britain across the equator during the Carboniferous 

(scotese and mcKerrow, 1990). Both the beginning and 

end of the Carboniferous period are marked by a climate 

that, at least seasonally, was in part arid. This led to the 

widespread development of commonly red, continental, 

alluvial, clastic-dominated facies during Tournaisian and 

late westphalian to stephanian times. The intervening time 

was dominated by an equatorial climate. 

The diverse lithofacies that developed throughout the 

Carboniferous were also the consequence of tectonic 

processes. A phase of late devonian to visean rifting 

produced a marked palaeorelief with numerous basins 

occupying subsiding grabens and half-grabens and emergent 

highs associated with horsts and tilt-block highs. Cessation 

of most rifting processes throughout large parts of Britain 

in the late visean was followed by a period of regional 

subsidence when the resulting basins were infilled by 

widespread deposits. 

1.1 TECTONIC SETTING 

The tectonic setting and palaeogeography of the 

Carboniferous of Great Britain was summarised by waters 

et al. (2007) (see also Browne et al., 1999 and Browne et 

al., 2003 regarding the midland valley of scotland and 

waters et al., 2009 regarding onshore southern Britain). For 

completeness, the sections in waters et al. (2007) that are 

relevant to onshore northern Great Britain, are reproduced 

here virtually intact. 

in the late devonian a phase of north–south rifting 

started to affect all of central and northern Britain, initiating 

the development of a series of grabens and half-grabens, 

separated by platforms and tilt-block highs (leeder, 

1982; 1988). From north to south these Carboniferous 

blocks and basins include the midland valley of scotland, 

Northumberland Trough, Alston Block, stainmore Trough, 

Askrigg Block and Craven Basin (Figure 1). The block 

and basin margins commonly reflected reactivation of preexisting 

basement lineaments. 

The midland valley of scotland is an east-northeast-trending 

complex graben, controlled by Caledonian 

basement structures. in the early devonian the graben was 

flanked to the north-west by the eroded remains of the 

Caledonian mountains north of the Highland Boundary 

Fault and to the south-east by the southern uplands southeast 

of the southern upland Fault. The midland valley 

of scotland was an active tectonic feature controlling 

sedimentation for much of the Carboniferous. depocentres 

within the graben subsided at different rates, and their 

locations and trend also changed (Browne and monro, 

1989). superimposed upon this are marked thickness 

variations resulting from synsedimentary movement on 

north-east- and east-trending faults in a strike-slip regime 

throughout the Carboniferous. Associated with this were 

minor phases of compression, most notably during the mid 

Carboniferous (Read, 1988). 

1 

The southern uplands separated the Northumberland 

Trough, including the Tweed and solway basins, from the 

midland valley of scotland. However, this barrier was 

breached by narrow basins of north-north-west trend. The 

solway–Northumberland Trough was bounded to the north 

by the North solway, Gilnockie and Featherwood faults 

and to the south by the maryport–Gilcrux–stublick–Ninety 

Fathom fault system. Both bounding structures were active 

during deposition (Chadwick et al., 1995). 

The Alston Block lies to the south of the Northumberland 

Trough. This horst is bounded to the south by the 

Closehouse–lunedale–swindale Beck faults, active during 

the Tournaisian–visean. The stainmore Trough, a halfgraben 

basin, lies immediately to the south, with the 

southern margin defined by the stockdale monocline 

(dunham and wilson, 1985). This structure also marks a 

transition in sedimentation between the basin and the tiltblock 

of the Askrigg Block to the south. The Craven Fault 

system defines the southern margin of the Askrigg Block. 

The manx–lake district Block occurs to the west of the 

Alston and Askrigg blocks and is separated from them by 

the broadly north–south trending strike-slip pennine–dent 

Fault system. 

Transtensional rifting continued to be active in the graben 

of the midland valley of scotland during the Namurian to 

stephanian. despite possible linkages to northern england 

across the southern uplands, the midland valley continued 

to evolve as a basinal entity distinct from the area to the 

south. 

Cessation of rifting during the late visean in the area 

between the southern uplands and the wales–Brabant 

massif resulted in a phase dominated by thermally induced 

subsidence during Namurian and westphalian times 

(leeder, 1982). The pennine Basin formed as part of this 

regional subsidence. 

1.2 PALAEOGEOGRAPHY 

The palaeogeographical reconstructions presented for 

the Carboniferous of Great Britain (Figure 2) have been 

adapted from those illustrated by Cope et al. (1992) and, 

for the midland valley of scotland, by Browne and monro 

(1989) and Read et al. (2002). 

1.2.1 Tournaisian 

in the midland valley of scotland axial flow of sediments 

from the south-west was established during the late 

devonian and continued into the early Carboniferous (Read 

and Johnson, 1967). The basin fill was composed largely 

of fluvial siliciclastic sediments transported along the 

axis of the graben, with significant contributions coming 

from the scottish Highlands to the north (Browne et al., 

1999). input from the southern uplands, to the south, was 

minor (Figure 2a). marine incursions were not common at 

this time. These strata were laid down whilst the climate 

was semi-arid and are characterised by the presence of 

calcareous and dolomitic pedogenic horizons (cornstones) 

formed on stable alluvial plains. during the mid Tournaisian 



a mudstone-dominated succession characterised by minor 

interbeds of ferroan dolostone beds (cementstones) and 

evaporites (mainly gypsum preserved) was deposited on 

alluvial plains and marginal marine flats (sabkhas) subject 

to periodic desiccation and fluctuating salinity. 

in northern england a series of gulf-like, tideless, 

hypersaline basins, including the Northumberland and 

stainmore troughs (leeder, 1992), developed between 

evolving horst and tilt-block highs (Figure 2a). The 

basins developed with variable influx from river systems, 

notably fluvial and deltaic input into the Northumberland 

Trough from the southern uplands. The ‘cementstone’ and 

‘cornstone’ deposits recognised in the midland valley are 

also developed along the southern margin of the southern 

uplands massif, linking with the midland valley in the area 

of the Cheviot Block. 

1.2.2 Visean 

in the midland valley of scotland during the early visean 

there was a major reversal of the axial palaeoslope and 

flow from the north-east became established (Greensmith, 

1965). volcanic rocks dominate in the western half of the 

midland valley (Figure 2b). in the east, the succession is 

largely fluviodeltaic and lacustrine (Browne and monro, 

1989), with the development of oil shales and freshwater 

limestones as minor, but important, components. These 

reflect the development of lakes characterised by the 

accumulation of abundant algal remains. during the late 

visean, the succession in the east of the midland valley 

was still dominated by fluviodeltaic and lacustrine 

deposits, but with intermittent marine incursions 

(Figure 2c) during the Asbian and the Brigantian. 

marine incursions, associated with the formation of thin 

limestones, were at their most frequent during the late 

Brigantian, when shelf seas intermittently covered much 

of the midland valley. 

The early visean depositional environment of the 

Northumberland Trough was dominated by lacustrine 

and fluviodeltaic clastic sedimentation. The main deltaic 

deposits were derived from the north-east and prograded 

gradually along the axis of the trough (Figure 2b). 

meanwhile, south of the Northumberland Trough, a period 

of marine transgression resulted in the establishment of 

platform carbonates, which gradually onlapped raised 

horst and tilt-block highs. during late visean times a 

cyclic succession of fluviodeltaic clastic rocks, marinereworked 

sandstones and shallow shelf marine carbonate 

rocks (‘yoredale’ facies) built up across northern england 

(Figure 2c), terminating deposition of the platform 

carbonates. 

1.2.3 Namurian 

The midland valley of scotland is characterised by a 

continuation of cyclic (‘yoredale’ facies) sequences with 



2 

interbedded fluviodeltaic clastic strata, coals and marine 

shelf limestones, the last mentioned marking highstands 

of sea level. This succession exhibits a progressive 

diminution of marine influence with time. Fluvial sediment 

input continued from the north-east (Figure 2d). during 

pendleian times, coal-forming environments with Lingula 

and nonmarine bivalves were common, but with intermittent 

marine incursions. The mid to late Namurian succession is 

characterised by alluvial deposits (Browne and monro, 

1989), with palaeosols. in parts of Northumberland, major 

sand bodies elongated parallel to the axis of the trough, 

occupy tectonically controlled erosive channels cut through 

the ‘yoredale’ facies succession (young and lawrence, 

2002). 

during pendleian times a fluviodeltaic system (‘millstone 

Grit’ facies) transported siliciclastic sediment into the 

northern margin of the Central pennine sub-basin, located 

to the south of the area covered by this report (see waters et 

al., 2009). equivalent, though more condensed, successions 

are recorded on the Askrigg Block and in the stainmore 

Trough. Although the term ‘millstone Grit’ is widely 

used on old geological maps of the north pennines and 

Northumberland, and remains embedded in the associated 

literature, the facies is absent from these areas. major 

distributary channels of pendleian and Arnsbergian age, 

present on the Alston Block (dunham, 1990), may represent 

the feeder channels for the fluviodeltaic successions found 

farther to the south. 

1.2.4 Westphalian 

From early in the westphalian a coal-forming delta-top 

environment became established across the midland valley 

of scotland and the pennine Basin. Although both ‘Coal 

measures’ cyclic successions are lithologically similar, the 

basinal areas were, largely, isolated by the raised area of 

the southern uplands. marine incursions were relatively 

rare during deposition of these successions (Figures 2e and 

2f), but those that did occur gave rise to widespread marine 

bands. 

Figure 1 (opposite) principal structural features of the 

northern British isles, onshore and offshore, that had 

significant influence on the deposition of Carboniferous 

strata. The depositional basins and highs shown are those 

that developed during the mississippian. Note that some 

post-Carboniferous structures are shown within the North 

sea to aid location of descriptions in the text. North sea 

structure is taken from Cameron (1993a and b) and Bruce 

and stemmerik (2003). see Figure 2 for 

palaeogeographical reconstructions through time. 

BH Bowland High; ClH Central lancashire High; dH 

derbyshire High; eG edale Gulf; HB Humber Basin; 

ldB lake district Block; mB manx Block; mvs midland 

valley of scotland.

58°N 

54°N 

Longford 

Down 

High 

0 

IRISH 

SEA 

N 

Firth 

of 

Clyde 

SOUTHERN UPLAND FAULT 

Peel Basin 

GREAT GLEN FAULT 

100 km 

MVS 

Southern 

Uplands 

Inner 

Moray 

Firth 

Grampian 

Highlands 

HIGHLAND BOUNDARY FAULT 

Solway Basin 

MB 

LAMMERMUIR FAULT 

Craven 

Basin 

LDB 

PENNINE 

FAULTS 

3 

Forth 

Approaches 

Basin 

Tweed 

Basin 

Northumberland 

Trough 

BH 

CLH 

Holme High 

Alston 

Block 

STUBLICK FAULT 

DENT FAULT 

Stainmore 

Trough 

Gainsborough 

Trough 

DH EG 

Widmerpool Gulf 

Hathern Shelf 

Land Shelf 

Basin 

Askrigg 

Block 

Outer 

Moray 

Firth 

UK CENTRAL 

NORTH SEA 

Western 

High 

Mid North 

Sea High 

UK SOUTHERN 

NORTH SEA 

Market 

Weighton 

Block 

Cleveland 

Basin 

FLAMBOROUGH HEAD FAULT 

N. CRAVEN 

FAULT 

MORLEY–CAMPSALL FAULT 

East 

Midlands 

Shelf 

4°W Wales–Brabant Massif 0° 

HB 

Tournaisian–Visean 

syn-rift fault 



Uplands 

60°N 

5°W 0° 

5°W 0° 

5°W 

0° 

a) Mid Tournaisian 

60°N b) Early Visean 

60°N c) Late Visean 

(Arundian) 

(Brigantian) 

Emergent areas 

Alluvial 

Alluvial 

‘Barren Measures’ lithofacies 

‘Coal Measures’ lithofacies 

Periodic marine 

influence 



V 

V 

MVS 

V 

V V 

MVS 

Alluvial 

‘Millstone Grit’ lithofacies 

SUM 

SUM 

V 

G-MH 

CB 

DB 

NT 

AIB 

AsB 

CB 

CLH 

V 

55°N 

NT 

CB 

55°N 

55°N 

V 

G-MH 

Alluvial 

AIB 

G-MH 

‘Yoredale’ and coastal lithofacies 

M-LD 

V 

AsB 

M-LD 

? 

V 

WT DH 

DB 

Alluvial 

plains 

CB 

? 

Hemipelagic lithofacies 

V 

V 

Wales–Brabant 

Massif 

SB 

V 

SB 

Platform and ramp carbonate lithofacies 

Wales–Brabant 

Massif 

Heterolithic clastic and 

nonmarine carbonate lithofacies 

V 

V 

V 

Continental and peritidal lithofacies 

50°N 

50°N 

50°N 

Principal direction of clastic input 

4 

0° 

60°N 

5°W 

f) Late Westphalian 

(Asturian) 

0° 

60°N 

5°W 

e) Early Westphalian 

(Langsettian) 

0° 

60°N 

5°W 

d) Early Namurian 

(Arnsbergian) 

Volcanicity 

V V V V V 

0 150 km 

Figure 2 palaeogeographic 

reconstructions for the Carboniferous of 

the British isles. Adapted from Cope et 

al. (1992). AlB Alston Block; AsB 

Askrigg Block; CB Craven Basin; CB 

Cheviot Block; CuB Culm Basin; dB 

dublin Basin; dH derbyshire High; 

G–mH Galway–mayo High; lH 

leinster High; m–ld manx–lake 

district Block; mvs midland valley of 

scotland; NT Northumberland Trough; 

sB shannon Basin; sT stainmore 

Trough; sum southern uplands 

massif; wT widmerpool Trough. 

V 

V 

V 

V 

SUM 

55°N 

55°N 

55°N 

G-MH 

SUM 

Pennine 

Basin 

Pennine 

G-MH 

G-MH 

V 

Basin 

Wales–Brabant Massif 

Wales–Brabant Massif Wales–Brabant Massif 

LH 

V 

Pennant 

CuB 

50°N 

50°N 

50°N

2 Correlation and biostratigraphical framework 

2.1 CHRONOSTRATIGRAPHY 

The Carboniferous system in western europe comprises 

two subsystems, an older dinantian and younger silesian, 

traditionally corresponding to lower Carboniferous 

and upper Carboniferous, respectively (Table 1). The 

dinantian–silesian boundary was chosen to represent 

a regional facies transition in Britain from dominantly 

carbonate (Carboniferous limestone supergroup) to 

terrigenous clastic strata and does not reflect a global 

change in flora or fauna. The lower boundary of the silesian 

is defined as the base of the ammonoid Cravenoceras leion 

Zone. 

The terms ‘dinantian’ and ‘silesian’ are now redundant 

and the mississippian and pennsylvanian of the usA 

have become recognised internationally as the only 

accepted main divisions (subsystems) of the Carboniferous, 

strictly representing the lower and upper Carboniferous, 

respectively, in international usage. The mid Carboniferous 

boundary separating the two subsystems occurs within 

the Chokierian stage of the Namurian series in western 

europe. 

difficulties in direct comparison between North 

America and western europe have resulted in Britain 

maintaining usage of the regional western european 

chronostratigraphical nomenclature. The new, official 

subdivision of the Carboniferous system, as voted for by 

the subcommission on Carboniferous stratigraphy, and 

ratified by the international Commission on stratigraphy 

and the international union of Geological sciences during 

the period 1999–2004, has not been applied to this report. 

However, the reader is referred to davydov et al. (2004) and 

Heckel and Clayton (2006) for further information. whilst 

the authors are fully aware of the changes to Carboniferous 

stratigraphical nomenclature, for sound practical reasons 

the old style has had to be maintained for the present. 

The dinantian is subdivided into the Tournaisian and 

visean series, whereas the silesian is subdivided into three 

series, the Namurian, westphalian and stephanian. These 

series do not represent global faunal or floral events, but 

were chosen to represent prominent facies variations in 

western europe. in northern Britain, the Tournaisian is 

dominated by continental and peritidal lithofacies, whilst 

the visean is largely represented in the midland valley of 

scotland by heterolithic clastic and nonmarine carbonate 

lithofacies, and in northern england by a mixture of open 

marine, platform and ramp carbonates, ‘millstone Grit’ and 

‘yoredale’ lithofacies. in northern Britain the Namurian is 

dominated by ‘yoredale’ and ‘millstone Grit’ lithofacies, 

and the westphalian is very largely represented by ‘Coal 

measures’ lithofacies. The base of the westphalian is taken 

at the base of the ammonoid Gastrioceras subcrenatum 

Zone, which broadly equates with the first incoming of 

thick coal seams. However, G. subcrenatum has not been 

found in scotland so the base of the westphalian there 

cannot be defined accurately. in scotland the base of the 

Coal measures is taken at the base of the lowstone marine 

Band, its local correlative, or at a plane of disconformity. 

The stephanian is restricted to strata of limited geographical 

extent in onshore northern Britain. 

5 

internationally, the Tournaisian and visean are now 

formally defined as stages, and work is in progress to 

define subsequent stages using nomenclatures defined 

in Russia. However, until this work is complete it is 

considered prudent to maintain usage of the well-established 

chronostratigraphical nomenclatures established in Britain 

and western europe. 

stage names for the visean, Namurian and westphalian 

are based on basal stratotypes defined by George et al. 

(1976) for the visean, Ramsbottom et al. (1978) for the 

Namurian, and owens et al. (1985) for the westphalian, 

largely from localities in northern england. The distribution 

at outcrop of the main chronostratigraphical units and the 

location of the stage stratotypes is shown in Figure 3. 

The stephanian series was originally defined in the 

massif Central of France with three stages, referred to 

as stephanian A, B and C. The stephanian A has been 

formally renamed the Barruelian stage. The recognition of 

a non-sequence in the massif Central and identification of 

an additional stephanian succession in Cantabria, northern 

spain, led to the recognition of a Cantabrian stage, which is 

older than the Barruelian. No strata of Cantabrian age have 

been recognised in northern Britain. 

2.2 BIOSTRATIGRAPHY 

Ammonoids (goniatites) are crucial to Carboniferous 

biostratigraphy, notably within the visean, Namurian and 

early westphalian series, where they provide the greatest 

biostratigraphical resolution. The nektopelagic habit of 

ammonoids allows biozones to be recognised across 

western europe and some are applicable globally. Thickshelled 

ammonoids occur within thin hemipelagic marine 

beds (known as ‘marine bands’), which developed during 

marine transgressions and typically comprise distinct 

ammonoid faunas. Ammonoid biozones are units defined 

by the successive first appearance of ammonoid taxa, 

with the base of the biozones coinciding with the bases 

of specific marine bands (Tables 2, 3 and 4). very little is 

known of the early Courceyan ammonoid faunas in Britain 

and ireland, and goniatite occurrences are rare in Britain 

in beds older than late visean. diagnostic goniatites are 

also uncommon in the Namurian of northern Britain, 

though work initiated by Currie (1954) showed that the 

classification of the pennines area could be applied to 

part, at least, of the scottish succession. Ramsbottom et 

al. (1978) applied a standard nomenclature based on the 

names of the principal diagnostic goniatites for the six 

most important marine bands in the coalfields of the British 

isles. Apart from the Cambriense marine Band, these 

bands can be traced throughout western europe, except in 

some marginal areas. 

Foraminifers are of biostratigraphical importance within 

Tournaisian and visean carbonates. They are particularly 

abundant in mid-ramp and platform settings, but also 

present within basinal deposits in limestone turbidites 

(Riley, 1993). The formal foraminiferal zonation for 

Belgium, established as the standard for north-west europe, 

has been applied to British and irish sequences by Conil et 



Table 1 Chronostratigraphical framework for 

the Carboniferous system of Great Britain. 

Ages derived from menning et al. (2000), 

davydov et al. (2004) (the dates shown in 

brackets are international stage boundary 

determinations from Gradstein and ogg, 2004); 

Carboniferous chronostratigraphy from Heckel 

and Clayton (2006); seismic sequences from 

Fraser et al. (1990); mesothems from 

Ramsbottom (1973, 1977a). 



Age 

(Ma) 

299 

(299.0 ± 0.8) 

(303.9 ± 0.9) 

(306.5 ± 1.0) 

310 

(311.7 ± 1.1) 

(318.1 ± 1.3) 

320 

330 

340 

(345.3 ± 2.1) 

350 

359 

(359.2 ± 2.5) 

6 

International 

Series 

KASIM- 

OVIAN 

PENNSYLVANIAN 

MISSISSIPPIAN 

International 

Stages 

GZHELIAN 

MOSCOVIAN 

BASHKIRIAN 

SERPUKHOVIAN 

VISEAN 

TOURNAISIAN 

European 

Subperiods 

European Stages 

(former Series) 

Heerlen 

Classification 

SILESIAN (UPPER CARBONIFEROUS) 

DINANTIAN (LOWER CARBONIFEROUS) 

STEPHANIAN 

WESTPHALIAN 

NAMURIAN 

VISEAN 

TOURNAISIAN 

C 

B 

A 

D 

C 

BARRUELIAN 

CANTABRIAN 

ASTURIAN 

BOLSOVIAN 

B DUCKMANTIAN 

A LANGSETTIAN 

C YEADONIAN 

MARSDENIAN 

B 

KINDERSCOUTIAN 

ALPORTIAN 

CHOKIERIAN 

A 

ARNSBERGIAN 

PENDLEIAN 

V3c BRIGANTIAN 

V3b ASBIAN 

V3a 

V2b 

V2a 

V1b 

V1a 

European Substages 

(former Stages) 

HOLKERIAN 

ARUNDIAN 

CHADIAN 

IVORIAN 

HASTARIAN 

COURCEYAN 

Seismic 

Stratigraphy 

V1 

LC2 

LC1 

EC6 

EC5 

EC4 

EC3 

EC2 

EC1 

Mesothems 

N11 

N9–10 

N6–8 

N5 

N4 

N3 

N2 

N1 

D6b 

D6a 

D5b 

D5a 

D4 

D3 

D2b 

D2a 

D1c 

D1b 

D1a

Ayrshire 

Mochrihanish 

Arran 

Sanquhar 

Basin 

54°N 

Thornhill 

Basin 

Isle of Man 

Solway 

Basin 

Volcanic rocks Warwickshire Group 

Coal Measures groups 

North Cumbria 

Central Coalfield Basin 

CHAPTER 4: MIDLAND VALLEY OF SCOTLAND 

CHAPTER 5: 

This report covers 

the area north of 

this line 

SOUTHERN UPLANDS 

West 

Cumbria 

Craven 

Basin 

S. Cumbria 

Furness & 

Cartmel 

al. (1980) and Conil et al. (1991) and is summarised in 

Table 2. 

Conodonts are present within marine facies, notably 

carbonate turbidites and hemipelagic shales, and conodont 

zones are particularly important for Tournaisian and visean 

correlation. varker and sevastopulo (1985) included 

zonations for both ‘shelf margin and basin facies’ and 

‘shelf facies’. Conodonts are also important in recognising 

the mid Carboniferous boundary and the base of the 

pennsylvanian subsystem. 

palynomorphs (miospores) are present in both marine 

and terrestrial environments and have been used for 

biozonation up to and including the Asturian (westphalian 

d) (Tables 2, 3 and 4). They are particularly useful 

for facilitating correlation in nonmarine rocks lacking 

stratigraphically useful macrofossils, and they can be used to 

correlate between nonmarine and marine sequences. Recent 

Namurian strata 

7 

Fife-Lothian Basin 

Tweed Basin 

CHAPTER 6: 

NORTHERN 

ENGLAND 

Cheviot Block / North-east 

Northumberland 

Northumberland Trough 

Alston Block 

4°W 0° 

Stainmore Trough 

Askrigg Block 

Tournaisian and Visean strata 

Regions covered by named 

chapters 

Figure 3 extent of Carboniferous rocks of onshore northern Great Britain. The approximate area covered by 

this report is indicated as is the location of regions discussed in the various chapters in the text. 

advances in macrofloral zonation show the importance of 

plant fossil biostratigraphy, particularly for the Asturian 

(westphalian d) and Cantabrian (Cleal, 1991). 

Coral/brachiopod biozonation has been of historical 

importance in the classification of Tournaisian and visean 

platform carbonates, though they are now considered strongly 

facies controlled. However, the zonation nomenclature of 

vaughan (1905) for Bristol and south wales and Garwood 

(1913) is still widely used and was summarised by George 

et al. (1976) and Riley (1993). Riley (1993, fig. 1) showed 

the interrelationship between the coral/brachiopod zones 

of vaughan (1905) and the modified conodont zones of 

varker and sevastopulo (1985) and the relationship of these 

and other zones to the former stages (now partly redefined 

substages) of the Tournaisian and visean. 

in the visean to Namurian, marine bivalves present 

within hemipelagic shales and occurring in association 

0 

N 

100 km 



Table 2 Tournaisian and visean biostratigraphical zonations, derived from Riley (1993). Grey shading 

indicates interzones (conodonts and miospores) or non-sequences (brachiopods). anch. bis. 

Scaliognathus anchoralis — Polygnathus bischoffi; Arnsb. Arnsbergites; B. Bollandoceras; bouc. 

Dollymae bouckaerti; bul. Eotaphrus bultyncki; bur. Eotaphrus burlingtonensis; C. Caninophyllum; coll. 

Gnathodus girtyi collinsoni; G. Goniatites; Gn. Gnathodus; has. Dollymae hassi; hom. Gnathodus 

homopunctatus; in. Polygnathus inornatus/Siphonodella; L. Lochriea; lat. Doliognathus latus; Lusit. 

Lusitanoceras; Lyrog. Lyrogoniatites; mono. mononodosa; Neoglyph. Neoglyphioceras; Parag. 

Paraglyphioceras; prae. Mestognathus praebeckmanni; Ps. Pseudopolygnathus; S. Siphonophyllia; Siph. 

Siphonodella; spic. Polygnathus spicatus; V. Vaughania; Z. Zaphrentis. 

Stages 

Visean 

Tournaisian (part) 

Substages 

Brigantian 

Asbian 

Holkerian 

Arundian 

Chadian 

late 

early 

Courceyan 

Gn.collinsoni Lyrog. georgiensis P2c 

L. mono 

Neoglyph. subcirculareP2b 

Lusit. granosus P2a 

Parag. koboldi 

Parag. elegans 

P1d 

P1c 

Gn.bilineatus Arnsb. falcatus P1b 

G. crenistria P1a 

G. globostriatus B2b 

G. hudsoni B2a 

L. commutata 

prae. 

anch. 

bis 

bur. 

lat. 

bul. bouc. 

Polygnathus mehli 

cf. 

has. 

bul. 

Ps. 

multistriatus 

Siph. 

Conodonts 

hom. 

spic. in. 

Beyrichoceras 

with ammonoids are of greatest stratigraphical importance 

(Riley, 1993). However, this lithofacies is unknown in the 

midland valley of scotland and is very rare in northern 

england. in the former region, the relatively diverse 

molluscan fauna is considered and treated as part of the total 

assemblage of macrofossils in marine facies. 

Nonmarine bivalves are fundamentally important to the 



Ammonoids 

B1 

B. hodderense 

Bollandites- 

Bollandoceras 

BB 

Fascipericyclus- 

Ammonellipsites 

FA 

Pericyclus 

Gattendorfia 

Foraminifera 

Neoarchaediscus Cf6 (part) 

Koskinotextularia- 

Pojarkovella nibelis 

Cf5 

Eoparastaffella Cf4 

Tetrataxis- 

Eotextularia 

Cf3 

Paraendothyra 

Cf2 

Chernyshinella 

Cf1 

 

 

 

 

 

 

2 

Mitchell 

(1981, 1989) 

K 

J 

I 

H 

G 

F 

E 

D 

C 

B 

A 

S. 

cylindrica 

1 

C. 

patulum 

Coral / brachiopod 

Z. delanouei 

V. vetus 

Vaughan 

(1905) 

Horizon 

E 

D2 

D1 

S2 (part) 

8 

D 

D2 

D1 

S2 

S2 (part) 

S1 S1 

C2 (part) 

C2 

C2 (part) 

C1 

Z 

K 

M 

Garwood 

(1913) 

C2 (part) 

C1 

Z? 

Miospores 

NC 

(part) 

VF 

NM 

TC 

TS 

Pu 

CM 

PC 

BP 

HD 

VI 

Macroflora 

Lyginopteris bermudensiformis / Neuropteris antecedens 

Triphyllopteris 

'Adianites' 

zonation of late Namurian and westphalian sequences in 

the midland valley of scotland and the Northumberland 

Trough (Table 4). They tend to occur in association with 

fish material and ostracods. 

estheriids are small crustaceans that occupied brackish 

waters. They can occur in prominent marker ‘bands’ in the 

westphalian.

Table 3 summary of the chronostratigraphical units of the Namurian and the main biozones for the 

most important fossil groups. 

EUROPEAN 

REGIONAL 

SUBSTAGE 

yeadonian 

marsdenian 

Kinderscoutian 

Alportian 

Chokierian 

Arnsbergian 

pendleian 

ZONE 

WESTERN EUROPEAN 

MARINE BANDS 

Index Ammonoid Ammonoid Index (Index) 

G 1b 

G 1a 

R 2c 

R 2b 

Cancelloceras 

cumbriense 

Cancelloceras 

cancellatum 

Bilinguites 

superbilinguis 

Bilinguites bilinguis 

Ca. cumbriense G 1b 1 

Ca. cancellatum G 1a 1 

Verneulites sigma R2c2 B. superbilinguis R2c1 B. metabilinguis R2b5 B.eometabilinguis R2b4 B. bilinguis R2b3 B. bilinguis R2b2 B. bilinguis R2b1 R 2a Bilinguites gracilis B. gracilis R 2a 1 

R 1c 

R 1b 

R 1a 

Reticuloceras 

reticulatum 

Reticuloceras 

eoreticulatum 

Hodsonites 

magistrorum 

R. coreticulatum R1c4 R. reticulatum R1c3 R. reticulatum R1c2 R. reticulatum R 1c 1 

R. stubblefieldi R1b3 R. nodosum R1b2 R. eoreticulatum R1b1 R. dubium R1a5 R. todmordenense R1a4 R. subreticulatum R1a3 R. circumplicatile R1a2 Ho. magistrorum R 1a 1 

H2c Vallites eostriolatus 

Homoceratoides 

prereticulatus 

V. eostriolatus 

H2c2 H2c1 H2b Homoceras undulatum H. undulatum H2b1 H 2a Hudsonoceras proteum Hd. proteum H 2a 1 

H 1b 

H 1a 

e 2c 

e 2b 

e 2a 

e 1c 

Homoceras 

beyrichianum 

Isohomoceras 

subglobosum 

Nuculoceras stellarum 

Cravenocera–toides 

edalensis 

Cravenoceras 

cowlingense 

Cravenoceras 

malhamense 

I. sp. nov. H1b2 H. beyrichianum H1b1 I. subglobosum H1a3 I. subglobosum H1a2 I. subglobosum H1a1 N. nuculum e2c4 N. nuculum e2c3 N. nuculum e2c2 N. stellarum e2c1 Ct. nititoides e2b3 Ct. nitidus e2b2 Ct. edalensis e2b1 Eumorphoceras yatesae e2a3 C. gressinghamense e2a2a Eumorphoceras 

ferrimontanum 

e2a2 C. cowlingense e2a1 9 

MIOSPORES CONODONTS 

Raistrickia fulva – 

Reticulatisporites 

reticulatus 

(FR) 

Crassispora kosankei – 

Grumosisporites 

varioreticulatus 

(Kv) 

Lycospora subtriquetra 

– Kraeuselisporites 

ornatus 

(so) 

C. malhamense e 1c 1 Bellispores 

nitidus – 

e1b Cravenoceras brandoni Tumulites pseudobilinguis e1b2 C. brandoni e1b1 e1a Emstites (Cravenoceras) 

leion 

E. leion e1a1 Lycospora subtriquetra 

– Kraeuselisporites 

ornatus 

(so) 

Stenzonotriletes 

triangulus – Rotaspora 

knoxi 

(TK) 

Reticulatisporites 

carnosus 

(NC) 

pars. 

Idiognathoides 

sinuatus – 


primulus 


corrugatus – 


sulcatus 

Declinognathus 

noduliferus 

Gnathodus bilineatus 

bollandensis 

Kladognathus 

– Gnathodus girtyi 

simplex 



Table 4 westphalian chronostratigraphy and biostratigraphical zonations. 

European 

Regional 

Substage 

Cantabrian 



Ammonoids Conodonts 

Donetzoceras 

Asturian cambriense 

oT 

Bolsovian 

duckmantian 

langsettian 

Donetzoceras 

aegiranum 

Anthracoceratites 

vanderbeckei 

Gastrioceras 

listeri 

Gastrioceras 

subcrenatum 


sulcatus parvus 


sinuatus – 


primulus (pars.) 

10 

Palynomorphs Non-marine bivalves 

Index Zone Zone Sub-zone 

sl 

NJ 

RA 

ss 

Thymospora 

obscura – 

T. thiessenii 

Torispora 

securis – 

T. laevignata 

Microreticulati- 

sporites nobilis – 

Florinites junior 

Radiizonates 

aligerens 

Triquitrites 

sinani- 

Cirratriradites 

saturni 

Anthraconauta 

tenuis 

Anthraconauta 

phillipsii 

‘Upper 

similis- pulchra’ 

‘Lower 

similis-pulchra’ 

Anthraconaia 

modiolaris 

Carbonicola 

communis 

Carbonicola 

lenisulcata 

adamsi-hindi 

atra 

caledonica 

phrygiana 

ovum 

regularis 

cristagalli 

pseudorobusta 

bipennis 

torus 

proxima 

extenuata 

fallax-protea

3 lithostratigraphical framework 

The plethora of local group and formation names and the 

inconsistent application of lithostratigraphical hierarchies 

for the Carboniferous has, to an extent, hindered the 

regional understanding of the Carboniferous successions of 

Great Britain. 

From an early, relatively simple framework, subsequent 

surveys and publications have greatly added to the complexity 

of the nomenclature. much of this existing nomenclature has 

evolved from work carried out long before guidance was 

available for best practice in lithostratigraphical procedures 

(Rawson et al., 2002). Consequently, a haphazard approach 

to the establishment of the hierarchy of units has resulted. 

The local nomenclatures can be attributed to the 

following: 

• restriction of deposits to individual basins 

• isolation by faulting or erosion of once laterally 

contiguous deposits following end Carboniferous and 

subsequent tectonic events 

• the former BGS methodology of mapping geological 

sheets in isolation 

• where a formal lithostratigraphical nomenclature has 

not been defined on BGs maps, scientific publications 

have created their own, commonly conflicting, 

schemes. 

The Geological society special Reports for the dinantian 

and silesian (George et al., 1976; Ramsbottom et al., 

1978) provided useful stratigraphical correlations between 

key sections across the British isles. However, the reports 

did not give a unified lithostratigraphical framework. 

Their preference was to promote a unified approach to 

lithostratigraphy, biostratigraphy and chronostratigraphy 

(Holland et al., 1978, p. 4). 

in order to review the existing nomenclature it was 

decided to follow the guidance of the North American 

stratigraphic Code (NAsC) (Anon., 1983) and more 

recently, Geological society of london guidance (Rawson 

et al., 2002), as these are commonly accepted standards. 

The nomenclature chosen should aid communication of 

British Carboniferous geology to others. However, it is 

acknowledged that many names are so entrenched in the 

literature that their replacement would result in confusion. 

As a consequence, this report uses existing nomenclature 

where suitable, whilst providing full definitions consistent 

with the guidance from the NAsC and the Geological 

society of london. 

An alphabetical listing of all the groups and formations 

present within northern Britain are provided in Appendix 

1. Redundant or obsolete names are listed in Appendix 3. 

3.1 GROUP FRAMEWORK 

in rationalising the stratigraphy it was decided to follow 

a ‘top-down’ approach by which the group nomenclature 

was based upon the recognition of major lithofacies. 

The committee considered the possibility of having a 

single group name for each lithofacies applicable to all 

Great Britain. However, the lithofacies were commonly 

11 

developed within distinct basinal areas and a single Britainwide 

group nomenclature would not aid the understanding 

of the evolution of the basins. Hence, it was agreed 

that separate group names should be employed for each 

distinct depositional area. where it was believed useful to 

provide a single term for a Britain-wide lithofacies, it was 

recommended it should be defined as a supergroup. 

Nine major lithofacies associations (Figure 4) have been 

identified for the Carboniferous of onshore Great Britain, 

all of which are recognised in the northern provinces. The 

main lithologies, environments of deposition, distribution 

and age ranges were first described by waters et al. (2007; 

see also Figure 2). 

A continental and peritidal facies is widespread across 

northern Britain including from the midland valley of 

scotland to central england. it was deposited from late 

devonian to visean times. There are two subfacies, which are 

commonly found to interdigitate. A continental fluvioclastic 

(‘cornstone’) subfacies commonly forms the first basin infill 

and extends onto horst and tilt-block highs. A peritidal marine 

and evaporite (‘cementstone’) subfacies is generally limited 

to troughs associated with grabens and half-grabens. 

A heterolithic clastic and nonmarine carbonate facies, of 

visean age, is principally present in the eastern part of the 

midland valley of scotland where it passes laterally westward 

into dominantly volcanic rocks. it is also present as 

early visean strata in parts of the Northumberland Trough. 

An open marine, platform and ramp carbonates facies 

accumulated during the visean on platforms and ramps that 

developed on horst blocks and half-graben tilt blocks over 

the Alston and Askrigg blocks, and fringing the manx–lake 

district Block. 

A hemipelagic facies was deposited in quiet and relatively 

deep basinal prodelta and carbonate slope environments 

that developed in the Furness and Cartmell area (south 

Cumbria) and the Askrigg Block–Craven Basin ‘Transition 

Zone’ during the early Namurian. 

A mixed shelf carbonate and deltaic (‘Yoredale’) facies 

is widespread across the midland valley of scotland and 

northern england as far south as the Craven Fault system. 

it is found in strata of visean to Namurian age. 

A fluviodeltaic (‘Millstone Grit’) facies extends from 

the midland valley of scotland, across northern and central 

england in strata of Namurian to early westphalian 

age. similar deposition may have occurred within the 

Northumberland Trough during early visean times. 

A fluviodeltaic (‘Coal Measures’) facies extends from 

the midland valley of scotland across northern england in 

strata of westphalian age. 

An alluvial (‘Barren Measures’) facies occurs as two 

subfacies in Britain (see waters et al., 2007). However, only 

the ‘red-bed’ subfacies occurs in northern Britain in west 

Cumbria, the ingleton Coalfield and the solway Basin. it 

was deposited during the westphalian. 

A volcanic facies is most thickly present as the Clyde 

plateau volcanic Formation (Arundian to Asbian) and 

Bathgate Group (Asbian to Arnsbergian) of the midland 

valley of scotland, but it is also significantly developed 

in the Tournaisian and visean age rocks of the solway and 

Tweed basins (Cockermouth, Birrenswark and Kelso vol- 



Principal lithofacies 

Volcanic lithofacies 

Barren Measures 

lithofacies 

Coal Measures lithofacies 

Millstone Grit lithofacies 

Yoredale lithofacies 


Platform/ramp carbonate 



nonmarine carbonate 


Continental and peritidal 


Mudstone/siltstone 



Grain size 

C SI FS CS Gr Cg 

Sandstone Dolostone 

Coal 

y 

y 

y 

y 

/ \ 

/ \ 

Description of principal lithologies 

Lava, tuff, tuffite, volcaniclastic sedimentary rocks and boles (fossil 

soils) 

Red, brown or purple-grey mudstone, siltstone, sandstone, 

conglomerate and breccia; minor coal, ‘Spirorbis limestone’ 

and calcrete. Also, grey sandstone to granulestone with subordinate 

grey mudstone and thin coal seams 

Black and grey mudstone, siltstone and sandstone, with common 

seatearth, thick coal seams and ironstone. Marine shale and other 

fossiliferous beds (’bands’), including those with nonmarine 

bivalves (’mussels’), Lingula and Planolites, may occur. 

Black and grey mudstone, siltstone and sandstone, with subordinate 

seatearth and thin coal seams, typically in upward-coarsening cycles 

Grey mudstone, siltstone, sandstone and marine limestone with 

subordinate seatearth and coal seams, typically in upward-coarsening 

cycles 

Dark grey to black mudstone with thin sandstone or marine limestone 

beds; subordinate breccia; sand- and carbonate-rich turbidite 

Blanket bioclastic carbonate, locally ooidal with common karstic 

bedding surfaces, or calcareous mudstone and bioclastic 

limestone, locally with mud mounds and patch reefs 

Grey sandstone, siltstone, mudstone and locally oil shale, with 

subordinate beds of lacustrine and some marine limestone and 

dolostone, coal, seatearth and ironstone 

Purple-red conglomerate, sandstone, siltstone and mudstone with 

nodules and thin beds of calcrete, or grey mudstone, siltstone and 

sandstone with dolostone, gypsum and anhydrite beds 

Lithology Sedimentary structures 

Limestone Cross-lamination 

Volcaniclastic 

12 

Planar lamination 

Rooted 

Mud mound 

Marine shale Lava Cross-bedding Calcrete 

y 

/ \ 

/ \ 

Mudstone intraclast 

Ooids 

Pebbles

canic formations), in the Namurian of the western midland 

valley (Troon volcanic member) and in Namurian to 

westphalian rocks of the eastern midland valley. 

it will be noted in the report that some groups designated 

in northern Britain may comprise two or more lithofacies 

associations (excluding volcanics). For example, in the case 

of the Clackmannan Group of scotland, this resulted from 

a desire not to have a large number of single-formation 

groups where several main lithofacies are represented, and 

in the case of the yoredale Group of northern england it 

dealt with local variances in the main lithofacies. 

3.2 FORMATION FRAMEWORK 

in most cases a nomenclature of formations, and to a lesser 

extent members, has been established. Those formations 

present within areas of recent geological resurvey already 

have a full formal lithostratigraphical description, which 

is replicated in this report. in some circumstances, the 

definition of existing formations has been revised, with the 

new definition reproduced in this report. some formations 

have been redefined as a group or member. elsewhere, it 

was decided that there was a requirement to rationalise 

several local formation names into a single unit. in these 

circumstances the new formation names generally utilise an 

existing, widely used name, which conforms to the NAsC 

criteria (Anon., 1983). in relatively few cases, formation 

names did not exist and new terms have been introduced as 

part of this study. 

A formation is a mappable unit that possesses internal 

lithological homogeneity or distinctive lithological features 

Figure 4 (Opposite) schematic graphic log summarising 

the nine main lithofacies. Although the lithofacies are shown 

broadly in their order of superposition, youngest at the top, 

they may interdigitate. The bases of the beds as shown are 

also highly schematic. C claystone; sl siltstone;Fs finegrained 

sandstone; Cs coarse-grained sandstone; Gr 

granulestone; Cg conglomerate. 

13 

that distinguish it from adjacent formations (see Rawson 

et al., 2002; Anon., 2005 for a full definition). individual 

coals, sandstones and limestones, whilst they may be ‘mappable 

units’ are treated as beds of informal level and are 

not described in this report. some limestones within the 

yoredale Group were considered to be amalgamated units 

of great lateral extent that warranted member status. 

The text in this report is largely based on entries in the 

BGs lexicon of Named Rock units for which lithological 

information has been compiled from many different sources 

using different classifications. where possible, limestone 

nomenclature uses the dunham (1962) scheme based on 

texture, modifying other terminologies where obvious. 

otherwise the Folk (1959; 1962) scheme, based mainly on 

composition, has been used. 

where possible, the nomenclature used for all igneous 

and sedimentary rock names follows the recommendations 

of the BGs Rock Classification scheme (RCs). However, 

in some circumstances it has been necessary to use the 

original descriptions and ‘legacy’ names. 

where relevant, the classification of basaltic rock in the 

midland valley of scotland devised by macGregor (1928) 

is included to permit comparison with previous maps and 

literature. To avoid repetition the six classes are listed here 

with their RCs-compatible translations for reference: 

Markle: plagioclase-macrophyric basalt to trachybasalt 

(hawaiite) 

Dunsapie: olivine-clinopyroxene-plagioclase-macrophyric 

basalt 

Craiglockhart: olivine-clinopyroxene-macrophyric basalt 

to basanite (referred to formerly as ankaramite) 

Jedburgh: plagioclase-microphyric basalt to trachybasalt 

(hawaiite) 

Dalmeny: olivine-microphyric basalt 

Hillhouse: olivine-clinopyroxene-microphyric basalt to 

basanite. 

These translations are compatible with the approach to 

rock classification and nomenclature set out in the BGs 

Rock Classification scheme (volume 1 igneous rocks) by 

Gillespie and styles (1999). 



4 Carboniferous rocks of scotland north of the southern 

upland Fault 

4.1 MIDLAND VALLEY OF SCOTLAND 

The group and formation nomenclature for the midland 

valley of scotland proposed by Browne et al. (1999) has 

been retained. There are four main groups, in ascending 

order, the inverclyde (partly devonian in age), strathclyde, 

Clackmannan and scottish Coal measures groups (Figure 5; 

see also Figure 6). The boundaries between the youngest 

three groups are defined by marker horizons that are 

widespread within the midland valley. volcanic rocks are 

common, ranging from thin local beds to widespread thick 

accumulations. The major occurrences of Carboniferous 

lavas are in the strathclyde and Bathgate groups. Those of 

the inverclyde and strathclyde groups exhibit a full range 

of compositions from basaltic to rhyolitic, whereas later 

magmatism was entirely basaltic or basanitic. 

4.2 INVERCLYDE GROUP (INV) 

The inverclyde Group (paterson and Hall, 1986) (Figure 5; 

see also Browne et al., 1999, fig. 1), of continental 

and peritidal facies comprises, in ascending order, the 

Kinnesswood, Ballagan and Clyde sandstone formations. 

it is characterised by sandstones with pedogenic carbonate 

(the continental and peritidal facies ‘cornstone’ subfacies) 

and by silty mudstones containing thin beds of dolostone 

and limestone (the continental and peritidal facies 

‘cementstone’ subfacies). There may be some lateral 

passage of the two subfacies. 

The base of the group is taken at the base of the 

Kinnesswood Formation where the dominantly sandstone 

lithologies of the underlying stratheden Group (late 

devonian: defined by paterson and Hall, 1986) are succeeded 

by pedogenic carbonate-bearing strata. Typically 

transitional, the base is locally defined by an unconformity 

in the west of the midland valley. The base of the 

strathclyde Group (heterolithic clastic and nonmarine carbonate 

facies) defines the top of the inverclyde Group, and 

the youngest formation, the Clyde sandstone Formation, 

that itself represents a return to fluviatile pedogenic facies 

similar to the basal Kinnesswood Formation. 

The type area of the inverclyde Group is Greenock, 

inverclyde district (see paterson and Hall, 1986). The 

group extends across the midland valley and occurs at 

machrihanish and on Arran, the Cumbrae isles and Bute 

and Cowal. it also extends across and along the southern 

margin of the ‘southern uplands Terrane’ from eyemouth 

to dalbeattie. Tournaisian (Famennian? to Chadian) in age, 

it is about 1500 m thick. 

4.2.1 Kinnesswood Formation (KNW) 

Name 

The name Kinnesswood Formation was introduced by 

Chisholm and dean (1974) and has since been extended 

throughout the midland valley of scotland and, by this 

report into the Northern england province (see section 

6.3.1). it replaces the former term ‘Cornstone Beds’, a unit 

at the top of the ‘upper old Red sandstone’. 



14 

Lithology 

in the midland valley of scotland the Kinnesswood 

Formation consists predominantly of purple-red, yellow, 

white and grey-purple, fine- to coarse-grained sandstones 

which are mostly cross-bedded and arranged in upwardfining 

units. Fine-grained, planar or poorly bedded 

sandstones, red mudstones and nodules and thin beds 

of concretionary carbonate (calcrete or ‘cornstone’) also 

occur. The cornstones range from immature, in which the 

sandstones have a partly carbonate matrix with ill-defined 

concretions, to mature, in which well-defined nodules 

(glaebules) are elongated in a vertical sense and are overlain 

by laminar and pisolitic structures. The laminar structures, 

which develop parallel to the bedding, may be brecciated 

and the carbonate replaced by chert. in the Northern 

england province the formation comprises mainly red 

sandstones, siltstones and conglomerates. 

Genetic interpretation 

in the midland valley of scotland the Kinnesswood 

Formation was laid down in fluviatile environments. The 

cross-bedded sandstones were deposited in river channels 

and the fine-grained sandstones and mudstones represent 

overbank deposits formed on the associated floodplains. 

The cornstones, which characterise the formation, were 

developed in soil profiles on the floodplains and channel 

margins under the influence of a fluctuating water table 

in a semi-arid climate. in the Northern england province 

the original sediments were laid down in calcrete-rich 

(cornstone) alluvial fans that were deposited in a series of 

small, linked basins with internal drainage that developed 

during early stages of crustal extension (Chadwick et al., 

1995). The beds are dominantly fluvial with a palaeocurrent 

towards the north-east. 

Stratotype 

The type section is the hillside to the east of the village 

of Kinnesswood at Kinnesswood Row, base of unit at 

[No 1805 0363], top at [No 1814 0362] (see Browne et 

al., 1999, fig. 1, col. 11). intra-Carboniferous erosion has 

removed the top part of the formation in the type area, but 

the BGs Glenrothes Borehole (BGs Registration Number 

No20se/385) [No 25617 03144] provides a complete 

reference section from 362.4 to 449.3 m depth (see Browne 

et al., 1999, fig. 1, col. 12). 

Lower and upper boundaries 

in the midland valley of scotland the transitional base 

of the Kinnesswood Formation is taken in the type area 

between strata with cornstones and the underlying aeolian 

sandstones without cornstones, the Knox pulpit Formation 

(stratheden Group). in most areas the top is conformable 

beneath the grey mudstone and siltstone with ferroan 

dolostones of the Ballagan Formation (Figure 6, Columns 

1–3, 4B), but in the type area it is erosional beneath strata 

of the strathclyde Group (pathhead Formation). 

in the Northern england province the base of the formation 

is typically unconformable upon silurian strata of 

the Riccarton Group. in the Berwick-upon-Tweed area 

and solway Basin, the Kelso volcanic and Birrenswark

Volcanic rock lithofacies 





nonmarine carbonate lithofacies 


Non-sequence 

CENTRAL 

COALFIELD BASIN 

volcanic formations respectively, overlie it (Figure 8, 

Column 12; Figure 10, Columns 2, 3). 

Thickness 

About 640 m (maximum) in the edinburgh area (based on 

mitchell and mykura (1962, p. 31), and up to 200 m thick in 

the Northern england province. Generally, 40 m on Arran 

Equivalent to the BATHGATE GROUP in Falkirk, Fife and Lanarkshire 

Groups and main lithofacies Groups and formations 

SCOTTISH 

COAL 

MEASURES 

GROUP 

CLACKMANNAN 

GROUP 

CLACKMANNAN 

GROUP 

STRATHCLYDE 

GROUP 

INVERCLYDE 

GROUP 

FIFE-LOTHIAN 

BASIN 

SCOTTISH 

COAL 

MEASURES 

GROUP 

CLACKMANNAN 

GROUP 

CLACKMANNAN 

GROUP 

STRATHCLYDE 

GROUP 

INVERCLYDE 

GROUP 

15 

CENTRAL 

COALFIELD BASIN 

SCOTTISH COAL MEASURES Gp 

CLACKMANNAN GROUP 

STRATHCLYDE GROUP 

INVERCLYDE GROUP 

SCOTTISH 

UPPER 

COAL 

MEASURES 

FORMATION 

SCOTTISH 

MIDDLE 

COAL 

MEASURES 

FORMATION 

SCOTTISH 

LCM 

FORMATION 

PASSAGE 

FORMATION 

PASSAGE 

Fm 

UPPER 

LIMESTONE 

FORMATION 

LIMESTONE 

COAL 

FORMATION 

LOWER 

LIMESTONE 

FORMATION 

LAWMUIR 

Fm 

CLYDE 

PLATEAU 

VOLCANIC 

Fm 

CLYDE 

SANDSTONE 

FORMATION 

BALLAGAN 

FORMATION 

KINNESS- 

WOOD 

FORMATION 

KIRKWOOD Fm 

FIFE-LOTHIAN 

BASIN 

SCOTTISH COAL MEASURES Gp 




SCOTTISH 

UPPER 

COAL 

MEASURES 

FORMATION 

SCOTTISH 

MIDDLE 

COAL 

MEASURES 

FORMATION 

SCOTTISH 

LCM 

FORMATION 

PASSAGE 

FORMATION 

PASSAGE 

Chronostratigraphy 

(BGs, 1987a), 68 m at Bute and Cowal, and 250 m in the 

Cumbrae isles (BGs, 2008). 

Distribution and regional correlation 

Throughout the midland valley, on Arran, at Bute and 

Cowal and in the Cumbrae isles. it is now extended across 

and south of the southern uplands from eyemouth to 

Fm 

UPPER 

LIMESTONE 

FORMATION 

LIMESTONE 

COAL 

FORMATION 

LOWER 

LIMESTONE 

FORMATION 

WEST 

LOTHIAN 

OIL- 

SHALE 

FORMATION 

GULLANE 

FORMATION 

ARTHUR’S SEAT 

VOLCANIC FORMATION 

CLYDE 

SAND- 

STONE 

BALLAGAN 

FORMATION 

KINNESS- 

WOOD 

FORMATION 

Figure 5 lithostratigraphical nomenclature for the midland valley of scotland. see section 3 for 

description of lithofacies, and Figures 6 and 10 for other localities discussed in text. This figure is not 

intended to name all the formations in the region. Fm formation; Gp group; lCm lower Coal measures. 

ASTURIAN 

BOLSOVIAN 

DUCKMANTIAN 

LANGSETTIAN 

YEADONIAN 

MARSDENIAN 

KINDERSCOU- 

TIAN 

ALPORTIAN 

CHOKIERIAN 

ARNSBERGIAN 

PENDLEIAN 

BRIGANTIAN 

ASBIAN 

HOLKERIAN - 

ARUNDIAN 

CHADIAN 

COURCEYAN 

FAMENNIAN 

WESTPHALIAN NAMURIAN VISEAN TOURNAISIAN 



4 

MIDLAND VALLEY 

OF SCOTLAND 

1 3 

2 

AGMB 

VDMB 

LOCALITIES 

A C 

N 

4 D E 

B SCOTTISH 

UPPER COAL 

5 

MEASURES 

FORMATION 

6 

M 

7 

SCOTTISH 

MIDDLE COAL 

MEASURES 

FORMATION 

M 



7 

SOLWAY 

SCOTTISH 

LOWER COAL 

MEASURES FM 

M 

SCOTTISH COAL MEASURES GP 

5 

SANQUHAR 

LOMB 

SBMB 

(position of) 

PASSAGE 

FORMATION 

98001782 

CAS 

PENNINE 

UPPER COAL 

MEASURES 

FORMATION 

UPPER 

LIMESTONE 

FORMATION 

6 

THORNHILL 

ILS 

CAMB 

PENNINE COAL 

MEASURES GROUP 

LIMESTONE 

COAL FM 

BLACK METALS MEMBER 


ARRAN 

1 

SCOTTISH 

UPPER COAL 

MEASURES 

FORMATION 

M 

PMCM 

M 

STAINMORE 

FORMATION 

SCOTTISH 

UPPER COAL 

MEASURES FM 

SCOTTISH 

MIDDLE COAL 

MEASURES FM 

GL 

L 

L 

M 

SCOTTISH 

MIDDLE COAL 

MEASURES FM 

L 

SCOTTISH COAL 


SCOTTISH MIDDLE COAL 

MEASURES FORMATION 

SCOTTISH COAL MEASURES 

GROUP (UNDIFFERENTIATED) 

SCOTTISH LOWER COAL 


PASSAGE FORMATION 

SCOTTISH COAL 

MEASURES GP 

PLCM 

KILBIRNIE 

MUDSTONE 

MEMBER 

ALSTON 

FORMATION 

SCOTTISH 

LOWER COAL 

MEASURES 

FM 

UPPER LIMESTONE FORMATION 

CMSC 

TOHO 

LOWER 

LIMESTONE FM 

CALS 

BASE OF HUR 

LIMESTONE COAL FM AND UPPER 

LIMESTONE FM (UNDIFFERENTIATED) 

LOWER LIMESTONE FORMATION 

CLACKMANNAN 

GROUP 

PASSAGE 

FM 

M 

TMB 

CLACKMANNAN 

GROUP 

ABERLADY 

WEST 

LOTHIAN 

OIL-SHALE 

FORMATION 

(HOPETOUN 

MEMBER) 

v PATHHEAD 

FORMATION 

M 

LAWMUIR 

FM 

CLOSEBURN 

LIMESTONE 

FORMATION 

(YOREDALE 

GROUP) 

CRAIGMADDIE MUIR 

SANDSTONE MEMBER 

ENTERKIN 

MUDSTONE 

FORMATION 

CLACKMANNAN 

GROUP 

FORMATION 

WBMB 

TYNE 

LIMESTONE 

FORMATION 

GULLANE 

FORMATION 


v 

SANDY 

v CRAIG 

FORMATION 

KINGHORN 

VOLCANIC 

FORMATION 

DOUGLAS MUIR QUARTZ- 

CONGLOMERATE MEMBER 

16 


VOLCANIC FM 

BULS 

KIRKWOOD 

FORMATION 

v v 

GV 

v 

v 

v 

WEST 

LOTHIAN 

OIL-SHALE 

FORMATION 

(CALDERS 

MEMBER) 

M 

SCMB 

PITTENWEEM 

FORMATION 

FELL 

SANDSTONE 

FORMATION 

SCALE 

STRATHCYLDE GROUP 


400 

GARLETON HILLS 

E VOLCANIC 

East FORMATION 

Lothian 

v CLYDE v 

PLATEAU 

VOLCANIC 

FORMATION 

v v 

LYNE 

FORMATION 

BORDER GROUP YOREDALE GROUP 

LIMESTONE COAL 

FORMATION 

LAWMUIR 

FORMATION 

CLYDE PLATEAU 

VOLCANIC FORMATION 

LAGGAN COTTAGE 

MUDSTONE FORMATION 

v v 

STRATHCLYDE 

GROUP 

MILLSTONE POINT 


LAGGANTUIN CORNSTONE 

MEMBER 

BALLAGAN FORMATION 

CLYDE 

SANDSTONE 

FORMATION 

INVERCLYDE 

GROUP 

200 

metres 

Base of 

Macgregor 

Marine Bands 


GULLANE 

FORMATION 

M 

ANSTRUTHER 

FORMATION 

‘SDV’ 

v 

ANSTRUTHER 

FORMATION 

v v 

FIFE NESS 

FORMATION 

v v 

CHARLES HILL 

VOLCANIC MEMBER 

v v 

v CLYDE 

PLATEAU v 

VOLCANIC FM 

BALLAGAN 

FORMATION 

INVERCLYDE GP 

0 


VOLCANIC 

FORMATION? 

Glasgow 

A 

3 

BUTE AND 

COWAL 


v 

CLYDE PLATEAU 

VOLCANIC FM 

v 

BIRGIDALE FM 

CYD 

ASCOG MEMBER 

(BUTE ONLY) 

BALLAGAN FM 

KINNESSWOOD 

FORMATION 

2 

GREAT AND 

LITTLE CUMBRAE 

KINNESSWOOD 

FORMATION 

STRATHCLYDE 

GROUP 

ELN 

CLYDE 

SANDSTONE 

FORMATION 

v v 

BIRRENSWARK 

VOLCANIC 

FORMATION 

KINNESSWOOD 

FORMATION 

C 

Central 

Fife 

MLC 

WBC 

v v 

ARTHUR’S 

SEAT 

VOLCANIC 

FORMATION 

v v 

KKS 

BALLAGAN 

FORMATION 

LSBU 

DRWN 

BROADLEE GLEN 


GOUROCK SANDSTONE 

MEMBER 

INVERCLYDE 

GROUP 

BALLAGAN FM 

FMN 

CLYDE 

SANDSTONE 

FORMATION 


KINNESSWOOD 

FORMATION 

INVERCLYDE GP 

KINNESSWOOD 

FORMATION 

DOUGHEND 

SANDSTONE 

MEMBER 

Edinburgh 

D 

Greenock-Dailly 

B 

Figure 6 Generalised vertical sections and correlation for Carboniferous strata in scotland. Based on lumsden et al. (1967), BGs (1987a), Browne et al. (1999), 

mcmillan (2002) and BGs (2008). The profiled location of the numbered and lettered sections is given in the inset map. see Appendices 1 and 2 for the names of 

the lithostratigraphical units shown by BGs lexicon of Named Rock units computer codes. m marine band; l Lingula band. v indicates named volcanic rock 

units; blue colour indicates named limestone beds; dashed lines indicate conjecture; wavy lines indicate unconformity surfaces.

dalbeattie, where it crops out narrowly along the northern 

margin of the Northumberland Trough in the langholm 

area (lumsden et al., 1967) and west of the Cheviot Hills. 

Age and biostratigraphical characterisation 

in the midland valley of scotland the formation is mostly 

early Carboniferous (Courceyan) in age, but the discovery 

of miospores of Tournaisian age (lN–pC biozones) from 

near the base of the formation (smith, 1996) confirms that it 

may straddle the devonian–Carboniferous boundary. in the 

Northern england province it is considered to be late devonian 

(Famennian) to early Tournaisian (Courceyan) in age, lumsden 

et al. (1967) and George et al. (1976) having postulated an early 

Carboniferous age for the upper part of the formation. 

Formal subdivisions 

see also Appendix 1. members of the Kinnesswood 

Formation, in ascending order, include: 

4.2.1.1 DougHenD sanDsTone MeMBer (DHs) 

Name 

previously named the dug Head sandstone member, which 

is considered to be a misspelling. see monro (1999); British 

Geological survey (2002a; 2002b; 2002c; 2005). 

Lithology 

mainly sandstone with a few cornstone concretions. 

Stratotype 

The type section comprises coastal exposures on the southwest 

side of Great Cumbrae island, North Ayrshire [Ns 

149 549 to 149 544]. There the boundaries with over and 

underlying strata are faulted, though they have been mapped 

as stratiform elsewhere across the island (see monro, 1999). 


The lower boundary is inferred to disconformably overlie redbrown 

sandstone of the late devonian Kelly Burn sandstone 

Formation, stratheden Group (Browne et al., 2001). 

The upper boundary is conformably overlain by redbrown 

silty mudstone, with carbonate-cemented concretions, 

of the Foulport mudstone member of the Kinnesswood 

Formation (Figure 6, Column 2). 

Thickness 

About 30 m. BGs (2008) gave a generalised thickness of 36 

m for the member. 


The doughend sandstone member is known only on the 

island of Great Cumbrae, where it is exposed on the southwest 

of the island in the vicinity of doughend Hole [Ns 149 

544]. The member is mapped at outcrop north-eastwards 

across the island. The outcrop is limited to the east by the 

Kaimes Bay Fault where the member is part of the hangingwall 

sequence. 

Age 

late devonian? 

4.2.1.2 FoulPorT MuDsTone MeMBer (FMn) 

Name 

From Foul port, millport Bay, Great Cumbrae, strathclyde. 

Lithology 

Red-brown silty mudstone with a few sandstones and beds 

with nodules of pedogenic limestone. see paterson and Hall 

(1986); BGs (in press); BGs (in preparation). 

17 

Stratotype 

The type area is the coast section at Foul port [Ns 157 546], 

millport Bay, Great Cumbrae, strathclyde. 


The lower boundary is conformable on the underlying 

doughend sandstone member. it is marked by a change 

from yellow sandstone with a few concretionary nodules to 

red-brown mudstone and siltstone of the Foulport mudstone 

member (monro, 1999; BGs in preparation). 

The upper boundary is conformable and overlain by 

variegated sandstones with concretions of the west Bay 

Cornstone member (Figure 6, Column 2). 


Cumbrae isles, strathclyde 

Thickness 

About 200 m. BGs (2008) gave a generalised thickness of 

198 m for the member. 

Age 

late devonian? to Courceyan 

4.2.1.3 wesT Bay CornsTone MeMBer (wBC) 

Name 

The west Bay Cornstone member is known from the south 

coast of the island of Great Cumbrae, adjacent to west Bay 

Road, millport. see monro (1999); BGs (2002a; 2002b; 

2002c; 2005). 

Lithology 

sandstone, yellow with red and green mottling, with 

carbonate-cemented (‘cornstone’) concretions. 

Stratotype 

The type section is coastal exposures on the southern side 

of Great Cumbrae island, strathclyde region. The entire 

member, including the lower and upper boundaries, is 

exposed on the coast at the south-west end of the town of 

millport [Ns 157 543 to 156 542] (see monro, 1999). 


The lower boundary conformably overlies the red-brown 

silty mudstone, with carbonate-cemented concretions, of 

the Foul port mudstone member, Kinnesswood Formation. 

The upper boundary is conformably overlain by a grey 

mudstone sequence with ferroan dolostone beds of the 

Ballagan Formation (Figure 6, Column 2). 

Thickness 

Approximately 16 m 


The west Bay Cornstone member is known only on the island 

of Great Cumbrae, where it is exposed on the south coast of 

the island adjacent to west Bay Road, millport. The member 

is mapped at outcrop to underlie the town of millport. The 

outcrop is limited to the east by the Kaimes Bay Fault where 

the member is part of the hanging-wall sequence. 

Age 

Tournaisian 

4.2.2 Ballagan Formation (BGN) 

Name 

The name Ballagan Formation was first introduced by 

Browne (1980) to replace the traditional term Ballagan Beds 



(or series), which referred, informally, to the mudstonecementstone 

sequence at Ballagan Glen (young, 1867 a, b). 

The name now encompasses strata in the lothians that 

were earlier (Chisholm et al., 1989) called the Tyninghame 

Formation (and in so doing acknowledges the presence of 

locally thick sandstones) and also part of the Cementstone 

Group of previous literature in Northern england, the 

Tweed Basin and the solway Basin (see peach and Horne, 

1903; Craig, 1956; Craig and Nairn, 1956; Nairn, 1956, 

1958) and part of the lower Border Group of lumsden et 

al. (1967). 

Lithology 

in the midland valley of scotland the Ballagan Formation 

is characterised by generally grey mudstones and siltstones, 

with nodules and beds (generally less than 0.3 m thick) 

of ferroan dolostone (‘cementstone’). Gypsum, and to a 

much lesser extent anhydrite, and pseudomorphs after 

halite occur. desiccation cracks are common and the rocks 

frequently show evidence of brecciation during diagenesis. 

Both these features are associated with reddening of the 

strata. Thin ripple-marked sandstones are present in many 

areas, and thick localised sandstones are also now included 

in the formation. in the Northern england province the 

Ballagan Formation comprises interbedded sandstone, 

mudstone, limestone (‘cementstone’) and anhydrite, the 

latter being present in the subsurface only. There are also 

pseudomorphs after evaporite minerals, some rootlet beds 

and thin coals. 


in the midland valley of scotland the Ballagan Formation 

formed in a peritidal environment associated with 

intermittent emergence. in the Northern england province, 

deposition of the formation was dominated by the influx 

of alluvial fans and fluvial and fluviodeltaic sediments 

from the southern uplands, intercalated with lacustrine 

and arid coastal plain deposits (deegan, 1973; leeder, 

1974). Hypersaline lacustrine and floodplain facies include 


and thin coals. 

Stratotype 

The partial type section, in the midland valley of scotland, 

is defined south of perth in the east dron Borehole (BGs 

Registration Number No11Nw/24) [No 1360 1572] from 

the bedrock surface at 15.26 to 224.80 m depth (see 

Browne et al., 1999, fig. 1, col. 7). The formation is also 

well exposed in Ballagan Glen [Ns 5731 8022]. in the 

Northern england province (see section 6.3.6 for full 

locality and stratigraphical details) partial type sections 

include disused quarries on whita Hill, the River esk from 

longwood to Broomholm, the River Annan from Rochell to 

Hoddom Castle, the Tarras water, Kirkbean Glen and the 

coastal section from port mary to Castle muir. A reference 

section occurs in the BGs Hoddom No.2 Borehole (BGs 

Registration Number Ny17se/3) [Ny1641 7285]. 


in the midland valley of scotland the base of the formation 

is taken at the lithological boundary between strata 

characterised by a mudstone–cementstone association 

and the underlying cornstone bearing sandstone of the 

Kinnesswood Formation (Figure 6, Column 4B). The top 

is drawn at the highest unit of mudstone and cementstone 

in any particular area. The mainly white sandstones of the 

Clyde sandstone Formation usually overlie the Ballagan 

Formation, except in parts of the lothians where the 



18 

mainly conformable base of the sandstones, mudstones and 

siltstones of the Gullane Formation, or volcanic rocks of the 

Arthur’s seat or Garleton Hills volcanic formations, overlie 

the Ballagan Formation. 

in the Northern england province the base of the formation 

is faulted or irregularly conformable upon the 

Birrenswark volcanic Formation in the solway Basin (Figure 

10, Columns 2, 3), it is conformable on the Kelso volcanic 

Formation in the Berwick area (Figure 8, Column 12), and 

elsewhere it is unconformable upon devonian and older strata. 

The top of the formation is presumed to be conformable 

beneath the lyne Formation of the Northumberland Trough 

and solway Basin (Figure 6, Column 7; Figure 10, Columns 

2, 3), but it is unconformable beneath the Fell sandstone 

Formation in the north-east part of the Northumberland 

Trough (Figure 8, Column 12; Figure 11, Column 1; Figure 

12, Columns 1, 2; Figure 13, Column 3). 

Thickness 

About 900 m (maximum) in the west lothian area (based 

on mitchell and mykura, 1962, p. 38), and up to 250 m 

thick in the Northern england province. Generally, 20 m on 

Arran (BGs, 1987a), 23 m in the Cumbrae isles and 38 m at 

Bute and Cowal (BGs, 2008). 


The formation occurs throughout the midland valley of 

scotland, on Arran, in the Cumbrae isles and at Bute and 

Cowal. it also also crops out in the north-eastern margins of 

the Northumberland Trough and at Kirkbean in the solway 

Firth area. in the central part of the Northumberland Trough 

a lateral facies change sees the Ballagan Formation pass 

into the lyne Formation of the Border Group. 


Tournaisian (Courceyan to Chadian). in the midland valley 

of scotland the Ballagan Formation typically contains 

miospores indicative of the Cm Biozone, although smith 

(1996) also recorded a sample from the pC Biozone. where 

present, the restricted fauna is characterised by the bivalve 

Modiolus latus, but ostracods are more abundant. in the 

Northern england province the fauna is also characterised 

by bivalves (including a modiolid fauna) and the annelid 

Serpula sp. 


see also Appendix 1. members of the Ballagan Formation 

in the midland valley of scotland, in ascending order, 

include: 

4.2.2.1 DruMwHirn MeMBer (Drwn) 

Name 

The member was previously referred to by eyles et al. 

(1949) as the ‘Basal sandstone’ of the Cementstone 

Group of the Calciferous sandstone measures. The present 

unit was named after drumwhirn Farm and defined by 

monaghan (2004). 

Lithology 

white-buff and yellow, medium- to fine-grained, thinly 

planar-bedded sandstone intercalated with finely laminated 

grey calcareous siltstone, calcareous mudstone, grey 

silty mudstone and rare, thin, nonmarine, muddy ferroan 

dolostone (‘cementstone’). 

Stratotype 

The type area is in the hills east and south of lindsayston 

Burn south-east of dailly between Craig and drumwhirn

farms and east of whitehill Farm [Ns 275 005 to 300 016] 

(see eyles et al., 1949; Floyd, 1999; monaghan, 2004). 


The basal contact is faulted in the type area (see above). The 

presence of grey silty mudstone and dolomitic limestone 

(‘cementstone’) interbedded with sandstone distinguishes 

this basal member of the Ballagan Formation from the 

underlying sandstone-dominated Kinnesswood Formation 

(Figure 6, Column 4B). 

The upper boundary is mapped as a conformable contact 

on 1:10 000 scale Geological sheet Ns20se in the 

lindsayston Burn section at [Ns 2824 0080] but is not 

actually exposed. The boundary is defined as the lithological 

change from yellow sandstone with grey silty mudstone 

to red-purple sandstone with conglomerate and pedogenic 

carbonate typical of the lindsayston Burn member. 

Thickness 

The member is at least 275 m thick in the type area (see 

above), but the base is faulted. The unit is interpreted to be 

of laterally variable thickness. 


The member occurs on 1:50 000 scale Geological sheets 

scotland 14w (Ayr) and scotland 8w (Carrick), and 

1:10 000 scale Geological sheets Ns20se and Ns30sw 

(part of) near dailly, south Ayrshire. The lateral extent of 

the unit is not yet finalised. 

Age 

Tournaisian (Courceyan) 

4.2.2.2 linDsaysTon Burn MeMBer (lsBu) 

Name 

After lindsayston Burn, south-east of dailly. The member 

was defined by monaghan (2004), having previously been 

referred to as ‘cornstone-bearing beds’ of the Cementstone 

Group of the Calciferous sandstone measures by eyles et 

al. (1949). see also Floyd (1999). 

Lithology 

Between [Ns 2821 0082 and 2272 0089], the strata are 

characterised by buff-white-grey, hard, flaggy sandstone, 

interbedded with soft red-green sandstone with pedogenic 

carbonate nodules and pipes, and rarer red-green siltstone 

and mudstone with pedogenic carbonate nodules. Thick 

channelised sandstone and conglomerate, a few metres 

thick and tens of metres wide, is observed at several 

localities. in the north-western part of the lindsayston Burn 

section [Ns 2272 0089 to 2749 0097] the upper part of the 

member records a gradational change. medium- to coarsegrained 

sandstone interbedded with red-grey siltstone with 

pedogenic carbonate is still common, but intercalations of 

grey calcareous siltstone and mudstone and thinly bedded 

fine-grained sandstone in packages up to about 0.7 m thick 

are also observed. 

Stratotype 

The type section occurs along the lindsayston Burn [Ns 

2824 0080 to 2735 0112], south-east of dailly on 1:10 000 

scale Geological sheet Ns20se (see eyles et al., 1949; 

monaghan, 2004). 


The lower boundary is defined as the lithological 

change from the underlying drumwhirn member of 

yellow sandstone with grey silty mudstone, to red-purple 

19 

sandstone with conglomerate and pedogenic carbonate 

(Figure 6, Column 4B). it is mapped as a conformable 

contact on 1:10 000 scale Geological sheet Ns20se in the 

type stream section at [Ns 2824 0080] but it is not actually 

exposed. 

The upper boundary is defined as the lithological change 

from red-purple sandstone with conglomerate and pedogenic 

carbonate, to the grey-green mudstone with thin nonmarine 

limestones and sandstone that is typical of the Ballagan 

Formation in the midland valley of scotland. it is mapped 

as a conformable contact on 1:10 000 scale Geological 

sheet Ns20se in the type stream section at [Ns 2735 0112] 

but it is not actually exposed. 

Thickness 

About 200 m at the type section (see above) with 134 m 

proved by logging where exposed. interpreted to be laterally 

variable and up to 285 m thick in other parts of 1:10 000 

scale Geological sheet Ns20se. 


The member occurs on 1:10 000 scale Geological sheets 

Ns20se, Ns20sw, and Ns30sw near dailly, south 

Ayrshire. The lateral extent of the unit is not yet known. 

Age 

Tournaisian (Courceyan) 

4.2.3 Clyde Sandstone Formation (CYD) 

Name 

From the River Clyde. The name Clyde sandstone 

Formation was introduced by paterson and Hall (1986) for 

sandstone-dominated strata, with ‘cornstones’, overlying 

the Ballagan Formation in the west of the midland valley. 

Lithology 

The Clyde sandstone Formation consists predominantly of 

white, fine- to coarse-grained sandstone, commonly pebbly, 

with beds of red-brown or grey mudstone. pedogenic limestone, 

as nodules or beds, and calcite cemented concretionary 

sandstones are also present in some areas. in more northerly 

areas some of the sandstones are conglomeratic, with pebbles 

of quartz and ‘Highland’ rock types (Browne et al., 1999). 

elsewhere the clasts are largely of intrabasinal limestone or 

mudstone. 


The strata were laid down in a wide range of fluviatile 

environments ranging from braided stream to floodplain 

with well developed overbank deposits. 

Stratotype 

The partial type sections (composite stratotype) of the 

Clyde sandstone Formation are in the Barnhill Borehole 

(BGs Registration Number Ns47Nw/2) [Ns 4269 7571], 

just east of dumbarton where the base and top of the 

formation occur at 161.5 and 104.9 m depth respectively, 

and in the Knocknairshill Borehole (BGs Registration 

Number Ns37sw/10) [Ns 3056 7438], east of Greenock, 

where the base and top of the formation occur at 222.9 and 

50.7 m depth respectively. 


The transitional base of the formation is taken at the 

lithological boundary between strata consisting 

predominantly of white sandstone with pedogenic 

limestone and the underlying mudstone and cementstone 



association of the Ballagan Formation (Figure 6, Columns 

1–3, 4B). The top is overlain variously by sedimentary or 

volcanic formations of the strathclyde Group. 

Thickness 

The maximum thickness is greater than 300 m in the 

Glasgow area (paterson and Hall, 1986, p. 11). 250 m on 

Arran (BGs, 1987a), 75 m at Bute and Cowal and 148 m in 

the Cumbrae isles (BGs, 2008). 


The Clyde sandstone Formation now extends throughout 

the midland valley and occurs on Arran, at Bute and Cowal 

and in the Cumbrae isles. it replaces the term Balcomie 

Formation (Browne, 1986) in Fife. The ‘upper sandstone’ 

of the pentland Hills (mitchell and mykura, 1962, p. 38) 

may also belong to it. 

Age 

late Tournaisian 


see also Appendix 1. members of the Clyde sandstone 

Formation in ascending stratigraphical order within the 

following geographical areas include: 

ISLE OF ARRAN 

4.2.3.1 lagganTuin CornsTone MeMBer (lgT) 

Name 

The member is named after laggantuin on the north-east 

side of the isle of Arran. see paterson and Hall (1986); 

GsGB (1924); Tyrell (1928). 

Lithology 

interbedded white sandstone and red claystone (shale) 

in fining-upwards cycles, with many small lenticular 

calcareous nodules (‘cornstone’) in the claystone. The upper 

beds recorded on the shore at laggantuin have fairly good 

continuous pedogenic nodular limestones about 0.3–0.6 m 

thick. The overlying upper part of the member, comprising 

thick-bedded white sandstone and pebbly sandstone, is 

exposed north of laggantuin. 

Stratotype 

The type section occurs in coastal exposures near laggantuin 

on the north-east side of the isle of Arran, strathclyde 

[Ns 0015 4855 to NR 9959 4914] (see paterson and Hall, 

1986). 


The lower boundary is mapped at the base of a white 

nodular limestone bed (‘cornstone’) that is approximately 

0.6 m thick, overlying the alternating sequence of grey 

mudstone (shale), nodular limestone (‘cornstone’) and 

thin grey sandstone that comprises the Ballagan Formation 

(Figure 6, Column 1). 

The upper boundary is conformably overlain by the pebbly 

coarse-grained white sandstone (grit) of the millstone 

point sandstone member. An occurrence of pebbly sandstone 

recorded as ‘millstone point Grits’ is exposed toward 

the northern part of the mapped extent of the laggantuin 

Cornstone member. 

Thickness 

Approximately 30 m. However, BGs (1987a) gave a 

generalised thickness of 50 m. 



20 


The vicinity of laggantuin, north-east coast of the isle of 

Arran, strathclyde. 

Age 

Tournaisian 

4.2.3.2 MillsTone PoinT sanDsTone MeMBer (MPs) 

Name 

From millstone point, north-east Arran. see paterson and 

Hall (1986). 

Lithology 

mainly white, cross-bedded sandstone with thin beds of 

red-brown or grey mudstone (BGs, 1987a). 

Stratotype 

The type section is the laggan shoreline on the north-east 

coast of the isle of Arran [NR 9995 4875 to 9887 5013]. 


The member conformably overlies the laggantuin 

Cornstone member (Figure 6, Column 1), which comprises 

sandstone and red-brown silty mudstone in fining-upward 

cycles with nodules and beds of concretionary limestone. 

The base is seen at [NR 9995 4875]. 

The stratigraphical top of the millstone point sandstone 

member is not seen. it is either faulted or unconformably 

overlain by grey mudstones with plant remains of the 

laggan Cottage mudstone Formation of the strathclyde 

Group. 

Thickness 

About 150–200 m. BGs (1987a) gave a generalised 

thickness of 200 m. 


laggan shoreline on the north-east coast of the isle of 

Arran. 

Age 

Tournaisian 

ISLE OF BUTE 

4.2.3.3 asCog MeMBer (aso) 

Name 

From Ascog, isle of Bute. The member was defined by 

paterson and Hall (1986). 

Lithology 

Red-brown siltstone and sandstone with pedogenic 

limestone. 

Stratotype 

The type section occurs in the BGs Ascog Borehole (BGs 

Registration Number Ns06se/8) [Ns 0986 6302] from 

133.6 to 219.8 m depth. 


At the lower boundary, sandstone of the Ascog member is 

interbedded with grey mudstone and dolomitic limestone 

(‘cementstone’) of the Ballagan Formation. The boundary is 

picked where beds of dolomitic limestone (‘cementstone’) 

are absent and sandstone becomes the predominant lithology. 

At the upper boundary there is a sharp change at the probably 

erosional base of the overlying Birgidale Formation, 

which comprises mudstone, sandstone, seatrock and coal.

Thickness 

some 86 m. However, BGs (2008) gave a generalised 

thickness of 75 m for the member on the isle of Bute. 


isle of Bute, strathclyde. 

Age 

Tournaisian 

CUMBRAE ISLES 

4.2.3.4 MillPorT CornsTones MeMBer (MlC) 

Name 

From millport, Great Cumbrae, strathclyde. 

Lithology 

Grey sandstone and red-brown silty mudstone with 

pedogenic limestone. see paterson and Hall (1986); monro 

(1999); BGs (in press); BGs (in preparation). 

Stratotype 

The type area is millport Bay [Ns 157 545], Great Cumbrae, 

strathclyde. 


The lower boundary is conformable (monro, 1999) and is 

described as ‘transitional’ (likely to be interbedded) with 

grey mudstone and dolomitic limestone of the Ballagan 

Formation (paterson and Hall, 1986) (Figure 6, Column 2). 

it crops out in millport Bay at [Ns 1561 5416]. 

The top of the member is not seen, but is presumed to 

be transitionally overlain by the eileans sandstone member 

that crops out on the eileans in millport Bay (paterson and 

Hall, 1986; monro, 1999). 

Thickness 

About 70 m. However, BGs (2008) gave a generalised 

thickness of 20 m for the formation. 


Cumbrae isles, strathclyde. 

Age 

Tournaisian 

4.2.3.5 eileans sanDsTone MeMBer (eln) 

Name 

Named after the eileans, millport Bay, Great Cumbrae, 

strathclyde. 

Lithology 

mainly white, cross-bedded sandstone (see paterson and 

Hall, 1986; BGs, in preparation). 

Stratotype 

The type area is the eileans [Ns 164 546], millport Bay, 

Great Cumbrae, strathclyde. 


Base not seen, but presumed transitional on the millport 

Cornstones member (Figure 6, Column 2). 

Top not seen, but presumed overlain by extrusive igneous 

rocks of the Clyde plateau volcanic Formation. 

Thickness 

About 150 m. However, BGs (2008) gave a generalised 

thickness of 128 m for the formation. 

21 


Cumbrae isles, strathclyde 

Age 

Tournaisian 

SOUTH OF THE RIVER CLYDE 

4.2.3.6 KnoCKnairsHill MeMBer (KKs) 

Name 

From Knocknairshill, port of Glasgow, strathclyde. 

Lithology 

mainly white or pale red cross-bedded sandstone with 

beds of red-brown silty mudstone; nodules and beds 

of pedogenic limestone (paterson and Hall, 1986). The 

member comprises well-developed upward-fining fluvial 

cycles including pedogenic carbonate (‘cornstone’) within 

the mudstone deposits in most cycles (paterson and Hall, 

1986; paterson et al., 1990; see also iGs, 1978). 

Stratotype 

A type section is exposed on the coast between Gourock 

and Clough, strathclyde [Ns 2340 7726 to 2082 7617]. 

An additional section occurs in the Knocknairshill BGs 

Borehole No. 4 (BGs Registration Number Ns37sw/10) 

[Ns 3056 7438] from 92.3 to 222.9 m depth (see paterson 

et al., 1990). 


The member at its lower boundary is interbedded with grey 

mudstone and dolomitic limestone (‘cementstone’) of the 

underlying Ballagan Formation (Figure 6, Column 4B). 

The base is picked where dolomitic limestone and grey 

mudstone beds are absent, and at the base of the first thick 

interval of sandstone containing medium, fining-upward 

beds of brownish grey, fine-grained sandstone and reddish 

brown, silty mudstone. 

The upper boundary of the member with the white crossbedded 

sandstones of the overlying Gourock sandstone 

member is mapped in the vicinity of Gourock Golf Course 

[Ns 2230 7630] but it is not exposed. in the Knocknairshill 

BGs Borehole No. 4 (see above) the member is unconformably 

overlain by volcaniclastic strata of the Clyde plateau 

volcanic Formation. 

Thickness 

The member is 130.58 m thick in the Knocknairshill BGs 

Borehole No. 4 (see above). 


The Greenock district south of the River Clyde to east and 

west of the largs Fault Zone, strathclyde. 

Age 

Tournaisian 

4.2.3.7 gouroCK sanDsTone MeMBer (gKa) 

Name 

From the town of Gourock on the south side of the Clyde 

estuary. previously known as the Gourock Formation. 

Lithology 

The Gourock sandstone member comprises white, crossbedded 

sandstone with thin beds of red-brown, silty 

mudstone, and nodules and beds of pedogenic limestone. 

it is distinguished from other units of the Clyde sandstone 



Formation by the presence of thicker beds of sandstone, a 

lesser proportion of mudstone and less abundant calcareous 

nodules (paterson and Hall, 1986; BGs, 1990). paterson 

et al. (1990) described the member as comprising thick 

multistorey bodies of white pebbly sandstone. 

Stratotype 

The type area is at [Ns 205 761] on 1:50 000 scale Geological 

sheet scotland 29e. 


The lower boundary of the member with the underlying 

Knocknairshill member (Figure 6, Column 4B) is mapped 

in the vicinity of Gourock Golf Course [Ns 2230 7630]. it 

is recognised by the presence of thick beds of white pebbly 

sandstone in the overlying Gourock sandstone member, but 

the boundary itself is not exposed. 

The upper boundary is not seen but it is presumed to be 

overlain by sandstone and mudstone strata of the Broadlee 

Glen sandstone member (paterson and Hall, 1986), which 

distinctively include plant debris and beds of grey mudstone 

(BGs, 1990). 

Thickness 

About 300 m. 


The Greenock district south of the River Clyde, and also 

west of the largs Fault Zone, strathclyde. 

Age 

Tournaisian 

4.2.3.8 BroaDlee glen sanDsTone MeMBer (Brlg) 

Name 

The member was previously known as the Broadlee Glen 

sandstones Formation. see paterson and Hall (1986); 

paterson et al. (1990); BGs (1990). 

Lithology 

Grey and white, cross-bedded sandstones with thin, lenticular 

beds of grey mudstone and carbonised plant debris (paterson 

and Hall, 1986; BGs, 1990). in the northern part of 

leapmoor plantation [Ns 221 715] the member consists of 

white and cream-coloured, trough cross-stratified sandstone 

with lenticular beds of grey siltstone and abundant coalified 

wood fragments (paterson et al., 1990). 

Stratotype 

The type area is Broadlee Glen near Greenock, strathclyde 

[Ns 2210 7150 to 2260 7140]. 


Base not seen. The member was mapped in Broadlee Glen 

[Ns 2258 7134] and distinguished from underlying strata of 

the undivided Clyde sandstone Formation by the presence 

of plant debris and beds of grey mudstone (BGs, 1990). 

paterson and Hall (1986) presumed that the unseen base 

of the Broadlee Glen sandstone member is transitional on 

white sandstones and red-brown mudstones of the Gourock 

sandstone member. 

Top not seen, but the Broadlee Glen sandstone member 

was presumed to be overlain by strata of the Clyde plateau 

volcanic Formation by paterson and Hall (1986) (Figure 6, 

Column 4B). 

Thickness 

Greater than 100 m. 



22 


south of the River Clyde and also west of the largs Fault 

Zone in strathclyde. 

Age 

Tournaisian. 

NORTH OF THE RIVER CLYDE 

4.2.3.9 overToun sanDsTone MeMBer (ovs) 

Name 

derived from overtoun, the member was previously 

known as the overtoun sandstone Formation (iGs, 1978). 

The present definition was published by paterson et al. 

(1990). 

Lithology 

The lower part of the overtoun sandstone member, 

approximately 36 m thick, is dominated by grey, finegrained, 

thin-bedded or partly concretionary sandstone. 

There are also intervals of mudstone, up to 3.3 m thick, 

commonly with calcareous concretions and uncommon 

beds of concretionary limestone or dolomitic limestone 

(‘cementstone’). The upper part, approximately 20 m thick, 

largely comprises pale grey, mostly fine-grained sandstone 

with clasts of carbonate. unlike the lower part of the 

member, sandstones with concretions and mudstones are 

uncommon. 

Stratotype 

The type section is the BGs Barnhill Borehole, near 

overtoun (BGs Registration Number Ns47Nw/2) [Ns 

4269 7571] from 104.89 to 161.48 m depth. 


The lower boundary of the member is conformable 

and overlies strata of the Ballagan Formation that are 

characterised by grey mudstone and dolomitic limestone 

(‘cementstone’). in the Barnhill Borehole (see above) 

the base is picked, at 161.48 m depth, at the top of a unit 

dominated by grey mudstone with gypsum veins, overlain 

by a sequence dominated by thick packages of sandstone. 

in the same borehole at 104.89 m depth, the upper 

boundary of the overtoun sandstone member is sharp and 

picked at a marked change from grey sandstone and mudstone 

to grey tuff, with volcanic lapillae, of the overlying 

Clyde plateau volcanic Formation. Correlation within the 

Greenock district demonstrates that the base of the Clyde 

plateau volcanic Formation is unconformable. 

Thickness 

some 56.6 m in the type section (see above). 


Area around overtoun House, north of the River Clyde near 

dumbarton, strathclyde. 

Age 

early visean. 

4.3 STRATHCLYDE GROUP (SYG) 

The ascending sequence of the strathclyde Group (paterson 

and Hall, 1986) (Figures 5, 6); see also Browne et al., 1999, 

fig. 2) includes: 

in the western Midland Valley of Scotland, the Birgidale, 

laggan Cottage mudstone, Clyde plateau volcanic, 

Kirkwood, and lawmuir formations;

in Fife, the Fife Ness, Anstruther, pittenweem, sandy 

Craig, and pathhead formations; 

in West Lothian, the Arthur’s seat volcanic, Gullane, 

and west lothian oil-shale formations. 

in East Lothian, the Garleton Hills volcanic, Gullane, 

and Aberlady formations. 

The group comprises mainly heterolithic clastic and 

nonmarine carbonate facies strata deposited in fluviatile, 

deltaic and lacustrine or lagoonal environments. 

lithologies are laterally variable. The sedimentary rocks 

consist of interbedded sandstone, siltstone and mudstone 

(including oil shales) with common seatearth, coal and 

sideritic ironstone. The volcanic successions comprise 

typically transitional to mildly alkaline lavas, pyroclastic 

rocks and volcaniclastic sedimentary rocks. Thin bioclastic 

limestone occurs within the uppermost part of the 

group that is characterised by the incoming of ‘yoredale’type 

cyclothems representing increasing marine conditions 

(Francis, 1991). 

The base of the group is taken, in Fife, at the conformable 

base of the Fife Ness Formation; in the lothians, at 

the mainly conformable base of the Gullane Formation 

or Arthur’s seat volcanic Formation; and in Central and 

western parts of the midland valley, at the sharp, irregular, 

unconformable base of the Clyde plateau volcanic 

Formation. The group represents a lithological change 

from the ‘cornstone’- and ‘cementstone’-bearing strata of 

the inverclyde Group to a seatrock and/or coal-bearing 

sequence in which volcanic rocks may be common. The 

base of the Clackmannan Group (mixed shelf carbonate and 

deltaic (‘Yoredale’) facies of a variable succession) defines 

the top of the strathclyde Group. 

The type area of the strathclyde Group is the Glasgow 

area of the strathclyde Region (see paterson and Hall, 

1986). Reference sections include coastal sections in east 

Fife, and the group extends across the midland valley 

of scotland to include machrihanish, the isle of Arran, 

the Cumbrae isles and Bute and Cowal. it also includes 

whitecleuch (leadhills, southern uplands). 

visean (Chadian to Brigantian) in age, the strathclyde 

Group exceeds 1250 m in thickness. paterson and Hall 

(1986) suggested it is about 1500 m thick in the type area. 

it may locally exceed 2000 m. 

WEST CENTRAL SCOTLAND (Arran, Bute and 

Cowal, and Glasgow) (Figure 6, Columns 1, 3 and 

4A) 

4.3.1 Birgidale Formation (BID) 

Name 

From Birgidale Knock Farm, south Bute, strathclyde 

Region (paterson and Hall, 1986). 

Lithology 

The Birgidale Formation consists of cyclically deposited 

grey mudstone, quartz pebble-bearing sandstone and 

seatearth with coal seams. 


The depositional environment was fluviodeltaic, mainly 

river channel and floodplains. 

Stratotype 

The type section is from 32.8 to 54.1 m depth in the 

Birgidale Knock Borehole (BGs Registration Number 

Ns05Ne/2) [Ns 0725 5990], the type area being around 

Birgidale Knock about [Ns 074 599] in south Bute. 

23 


The base of the formation is sharp, probably erosional, 

on the Ascog member of the Clyde sandstone Formation 


The top is overlain by lava, tuff and volcaniclastic sedimentary 

rocks of the Clyde plateau volcanic Formation. 

Thickness 

About 16 m (paterson and Hall, 1986, p. 13). However, 

BGs (2008) gave a generalised thickness of 25 m for the 

formation. 


isle of Bute 

Age 

visean 

4.3.2 Laggan Cottage Mudstone Formation (LNT) 

Name 

Taken from laggan Cottage, north-east Arran (paterson and 

Hall, 1986, p.14). 

Lithology 

The laggan Cottage mudstone Formation consists of grey 

carbonaceous mudstone with subordinate sandstones. plant 

remains occur but no coal seams are developed. 


The depositional environment was fluviodeltaic, mainly 

floodplain or lacustrine. 

Stratotype 

The type area is in the neighbourhood of laggan Cottage, 

north-east Arran [NR 986 501] where the entire thickness 

of the formation is present. 


The base of the formation is taken at the faulted or 

unconformable top of the white sandstone forming the 

millstone point sandstone member of the Clyde sandstone 

Formation at [NR 9887 5013] (Figure 6, Column 1). 

The formation is overlain by lava and tuff of the Clyde 

plateau volcanic Formation at [NR 9855 5035]. 

Thickness 

About 7 m (paterson and Hall, 1986, p.14). However, BGs 

(1987a) gave a generalised thickness of 10–20 m. 


North-east Arran 

Age 

visean 

4.3.3 Clyde Plateau Volcanic Formation (CPV) 

Name 

Taken from the River Clyde. The name was introduced by 

monro (1982) to replace earlier terms such as the Clyde 

plateau lavas. 

Lithology 

The Clyde plateau volcanic Formation consists of 

lavas, pyroclastic rocks and volcaniclastic sedimentary 

rocks. The lavas are transitional to mildly alkaline and 

show a wide range in composition. The ‘basic’ rocks 



are mostly hypersthene-normative with a few being 

silica-undersaturated nepheline-normative. The morefractionated 

rocks are almost all quartz-normative in 

composition, although rare nepheline-normative trachytic 

lavas have been identified and phonolitic rocks form some 

intrusions. The range in rock type is olivine+pyroxenephyric 

basalt and basanite–olivine+clinopyroxene+pl 

agioclase-phyric basalt–plagioclase-phyric hawaiite– 

mugearite–benmoreite–trachyte–rhyolite. Benmoreite is 

rare and the end members of the range are uncommon. 

in the north-west part of the midland valley, in the 

Kilpatrick–Campsie–Gargunnock blocks, the sequence is 

dominated by plagioclase-phyric hawaiites. plagioclasephyric 

basalts are less abundant and clinopyroxene-phyric 

types are uncommon. in the south-western part of the 

midland valley, Renfrewshire Hills and lanark blocks, a 

full range of compositions and petrographical variations 

are present. 


The formation was produced by one major episode of subaerial 

volcanic activity. 

Stratotype 

The type area is Campsie Glen [Ns 6098 8001] where 

the local base is in exceptionally sharp contact with the 

underlying Ballagan Formation (rather than the Clyde 

sandstone Formation). The lawmuir 1A Borehole (BGs 

Registration Number Ns57sw/162) [Ns 5182 7309], west 

of Bearsden in Glasgow, provides a partial type section 

where the top of the formation occurs at 281.12 m, shortly 

above the bottom of the hole at 286.5 m depth. 


The base of the formation is taken at the lithological 

change from the underlying clastic sedimentary rocks 

into lava, tuff or volcaniclastic sedimentary rocks. This 

contact, where seen, is normally sharp, representing a 

gentle but irregular unconformity. locally, the formation 

is underlain by the Birgidale Formation on Bute, and by 

the laggan Cottage mudstone Formation on Arran (Figure 

6, Columns 3, 1). 

The top is marked by a change to the volcaniclastic 

sedimentary rocks of the Kirkwood Formation (Figure 6, 

Column 4A). 

Thickness 

The maximum thickness exceeds 420 m in the Campsie 

Fells (Forsyth et al., 1996, p. 9). paterson and Hall 

(1986, p.13) suggest up to 800 m. it may be more than 

900 m thick in the Renfrewshire Hills (paterson et al., 

1990). more than 40 m thick in the main coalfield area at 

machrihanish (BGs, 1996). Generally 70–80 m thick on 

the isle of Arran (BGs, 1987a). 150 m and 175 m thick 

at Bute and Cowal and in the Cumbrae isles respectively 

(BGs, 2008). 


western midland valley of scotland, on Arran, at Bute and 

Cowal, in the Cumbrae isles and at machrihanish. 

Age 

mid visean (Arundian to Asbian). 


see also Appendix 1. members of the Clyde plateau 

volcanic Formation in approximate stratigraphical order 

within the following geographical areas include: 



24 

RENFREWSHIRE HILLS (including the Kilburnie Hills) 

4.3.3.1 noDDsDale volCaniClasTiC MeMBer 

Name 

previously named the Noddsdale volcaniclastic Beds 

(paterson et al., 1990, monro, 1999). part of the ‘lower 

Group’ of Richey (1928) and ‘unit 1’ of Johnstone (1965). 

Lithology 

purple basaltic tuff, agglomerate and pyroclastic-breccia with 

some bedded volcaniclastic sandstone. A complete section 

through the unit is recorded in the largs Borehole (BGs 

Registration Number Ns25Nw/5) [Ns 2158 5936] with 

about 44 m of volcanic detritus, fine- to coarse-grained with 

basaltic lava blocks up to 0.2 m long, bedded in places. Finegrained 

with accretionary lapilli in basal 3 m. The volcanic 

detritus is underlain by 11 m of silty mudstone and then 7 m 

of tuffaceous sandstone containing clasts of lava and quartz. 

Clasts of lava in sandstones and agglomerates are locally 

derived. Fine-grained tuffs are commonly well bedded and 

grade into water-laid volcaniclastic and quartzose sandstones 

containing some carbonised plant debris. 

Stratotype 

The type section comprises a complete sequence, about 

62.1 m thick, through the Noddsdale volcaniclastic member 

in the largs Borehole (see above) from about 107.4 to 169.5 

m depth. see description above and paterson et al. (1990). 


in the area between loch Thom [Ns 26 72] and largs 

[Ns 20 59] east of the largs Fault-zone, the basal tuffs, 

agglomerates and breccias of the Noddsdale volcaniclastic 

member rest upon ‘cornstone’-bearing sandstones of the 

Kinnesswood Formation. Farther north and to the west of 

the largs Fault-zone between outerwards Reservoir [Ns 

232 654] and Rottenburn Bridge [Ns 25 69], the Noddsdale 

volcaniclastic member overlies strata from the Clyde 

sandstone Formation of late devonian to Tournaisian to 

early visean age. This basal contact represents a regional 

erosional unconformity prior to the onset of the mid visean 

volcanism in the Renfrewshire Hills. 

The tuffs, agglomerates and pyroclastic breccias of the 

Noddsdale volcaniclastic member are overlain by the olivine-microphyric 

basalt (‘dalmeny’) lavas of the largs lava 

member. in the largs Borehole (see above) about 107 m of 

grey feldspar-phyric lava of the largs lava member overlie 

the volcaniclastic sedimentary rocks of the Noddsdale 

volcaniclastic member. 

Thickness 

Between 0 and 200 m. 


Renfrewshire and Kilbirnie hills. The member forms the base 

of the Clyde plateau volcanic Formation in the area between 

loch Thom [Ns 26 72] and largs [Ns 20 59]. it does not 

crop out south of largs but is inferred to occur beneath the 

largs lava member as far as the A760 road [Ns 21 57]. 

Age 


4.3.3.2 largs lava MeMBer 

Name 

previously named the largs lavas (paterson et al. 1990, 

monro 1999), part of the ‘lower Group’ of Richey (1928), 

and part of ‘unit 2’ of Johnstone (1965).

Lithology 

olivine-microphyric basalt lavas (‘dalmeny’ type) 

with a few flows of clinopyroxene-olivine-microphyric 

basalt (‘Hillhouse’ type). some clinopyroxene-olivinemacrophyric 

basalts or basanites are intercalated in the 

upper part of sequence. 

Stratotype 

The type area of the member occurs as a major scarp on 

the east side of Noddsdale, to the south of the muirshiel 

Fault, which can be traced northwards along the east side of 

Noddsdale water to the Rotten Burn [Ns 252 682]. 


The largs lava member overlies the Noddsdale 

volcaniclastic member. in the largs Borehole (BGs 

Registration Number Ns25Nw/5) [Ns 2158 5936] from 

about 8.2 to 107.4 m depth, the lavas of the largs lava 

member overlie the volcanic detritus, silty mudstone 

and tuffaceous sandstone of the Noddsdale volcaniclastic 

member. south of largs [Ns 20 59] the largs lava 

member is not exposed, but is inferred to occur beneath the 

Greeto lava member (monro, 1999). 

lavas of the largs lava member are more mafic 

than those of the overlying Greeto lava member with 

the boundary defined by the petrographical change from 

olivine-microphyric basalts (‘dalmeny’ type) of the largs 

lava member, to the plagioclase-phyric basalts and hawaiites 

(‘Jedburgh’ and ‘markle’ types) of the Greeto lava 

member. 

Thickness 

up to 130 m 


Renfrewshire and Kilbirnie hills: the member occurs as a 

scarp slope east of Noddsdale water from largs [Ns 21 

58] to the murishiel Fault [Ns 23 65], on the eastern side 

of Knockencorsan Hill [Ns 24 67], and south of largs on 

the lower slopes of douglas park as far as the A760 road 

[Ns 21 57]. 

Age 


4.3.3.3 greeTo lava MeMBer 

Name 

The name is derived from exposures in the valley of the 

Greeto water. previously named the Greeto lavas (paterson 

et al. 1990, monro 1999). part of the ‘lower Group’ of 

Richey (1928) and part of ‘unit 2’ of Johnstone (1965). 

Lithology 

plagioclase-microphyric basaltic to hawaiite lava (‘Jedburgh’ 

type) with a few flows of plagioclase-macrophyric basaltic 

to hawaiite lava (‘markle’ type). At the base of the member 

in the Kilbirnie Hills thin beds of purple nodular tuff with 

intercalated fine-grained red ‘marls’ are developed locally, 

for example east and south-east of Bradshaw [Ns 240 530]. 

A single flow of more-mafic olivine-pyroxene-macrophyric 

basalt or basanite occurs within the member on the north 

slope of Castle Hill at largs [Ns 220 589] 

Stratotype 

A reference section is well exposed in the valleys of the 

Greeto and Gogo waters, close to their confluence [Ns 230 

593]. 

25 


The member is underlain by the more-mafic olivinemicrophyric 

basalts (‘dalmeny’ type) of the largs lava 

member. 

it is overlain by the aphyric mugearites and olivine-free 

plagioclase-macrophyric hawaiites (‘markle’ type) of the 

strathgryfe lava member. 

Thickness 

up to 110 m in the largs area 


Renfrewshire and Kilbirnie hills: crops out extensively 

along the top of the scarp slope east of Noddsdale water 

from largs [Ns 210 590] north to the muirshiel Fault. 

exposed in the valley of the Greeto water [Ns 230 600]. To 

the south of largs the Greeto lava member forms a scarp 

feature at the top of the hills behind largs and Fairlie [Ns 

230 550]. The scarp extends south-south-east on the east 

side of the Caaf water valley [Ns 230 530]. The member 

is about 100 m thick in the largs area but thins southwards 

and lenses out at wardlaw [Ns 250 510]. An outlier caps 

Kaim Hill [Ns 220 530] to the west of the Caaf water 

valley. 

Age 

mid visean (Arundian to Asbian) 

4.3.3.4 MisTy law TraCHyTiC MeMBer 

Name 

previously named the misty law Trachytic Centre (paterson 

et al., 1990). part of the ‘lower Group’ of Richey (1928) 

and part of ‘unit 3’ of Johnstone (1965). 

Lithology 

The member comprises trachyte and rhyolite lavas with 

associated volcaniclastic rocks, including pyroclastic 

breccia and tuff, minor amounts of trachyandesite and 

trachybasalt (capping Totterie law [Ns 293 621]) and one 

major basaltic intercalation. 

Stratotype 

Reference sections or type areas are described for six main 

phases of the extrusive activity: 

1 Trachyte lavas exposed in streams south-east of 

waterhead moor [Ns 263 621] and around the 

headwaters of the River Calder; 

2 pyroclastic rocks in the scarp to the east of waterhead 

moor [Ns 269 624], also in Gogo Burn, Routdane 

Burn, murchan Burn [Ns 290 609] (including lenses 

of carbonaceous mudstone and plant fragments) and 

surge Burn; 

3 Trachytic lavas and welded tuffs forming high land 

that extends north and north-east from the Gogo water 

headwaters [about Ns 264 596]; 

4 Basaltic and intermediate lavas forming outliers in 

The Tongue [Ns 280 610] and more continuous 

outcrops around east Girt Hill [Ns 279 627], Burnt 

Hill [Ns 270 634] and Queenside loch [Ns 292 

642]; 

5 massive flows of trachyte and rhyolite overlying the 

basic lavas on and west of Queenside Hill [Ns 293 

638], on Hill of stake [Ns 274 630] and south-east 

from east Girt Hill [Ns 279 627] to little misty law 

[Ns 299 621]; 

6 Trachyandesite and trachybasalt capping Totterie law 

[Ns 293 621] and misty law [Ns 295 620]. 




Along the western margin of the ‘centre’, the contact of 

the misty law Trachytic member with the underlying 

strathgryfe lava member is not exposed but appears to be 

conformable and to dip gently to the south-east. 

The more steeply dipping upper boundary of the misty 

law Trachytic member is believed to be overstepped by the 

overlying lavas of the strathgryfe lava member but, where 

exposed, the contacts are generally faulted. unfaulted junctions 

are seen only in the River Garnock [Ns 293 593] and 

in the Rough Burn [Ns 315 617]. 

The distal parts of the cone, where it interdigitates with 

more mafic rocks, are mainly obscured by faulting but may 

be represented by thin developments of trachyte and trachytic 

tuff at south Burnt Hill [Ns 255 651], Feuside Hill [Ns 

252 597] and at lang Hill [Ns 250 612]. 

Thickness 

up to 300 m. 


in the Renfrewshire Hills, the member’s outcrop is 8 km 

wide in the area around misty law [Ns 295 620], extending 

from the headwaters of the River Calder [Ns 258 646] in 

the north-west, to muirshiel Country park [Ns 315 630] in 

the south-east, to the Knockside Hills [Ns 256 582] in the 

south. 

Age 


4.3.3.5 sTraTHgryFe lava MeMBer 

Name 

The member is named after the valley of the Gryfe water. 

it was previously referred to as the strathgryfe lavas (with 

informal lower and upper parts) by paterson et al. (1990). 

part of the ‘lower Group’ of Richey (1928) and ‘unit 3’ 

of Johnston (1965). see also monro (1999); stephenson in 

stephenson et al. (2003). 

Lithology 

Aphyric lava (mugearites) and olivine-free plagioclasemacrophyric 

hawaiite lava (‘markle’ type), in roughly 

equal proportions and commonly in composite flows. 

Thin olivine-pyroxene-macrophyric basalt lava and olivinebearing 

plagioclase-macrophyric basalt (‘markle’ type) 

occur in the upper part of the member. Boreholes near 

Clovenstone [Ns 33 16] show individual flows between 

3 and 20 m thick, with an average of about 10 m. in the 

boreholes, the flows are almost invariably separated by 

boles (dark red weathered horizons, fossil soil), up to 1 m 

thick, which are rarely seen at outcrop. most flows contain 

layers of fresh, massive lava, amygdaloidal lava and 

hydrothermally altered, autobrecciated, ‘slaggy’ material. 

The altered and slaggy material is commonly soft, friable 

and in some cases makes up 90 per cent of the flow. 

Stratotype 

The type area includes a large number of site investigation 

boreholes that were drilled around the River Calder [Ns 

3244 6165]. These boreholes penetrated the ‘markle’ type 

basalt and mugearite of the strathgryfe lava member down 

to 60 m. Geological logs of the boreholes are available 

together with a site investigation report. A reference section 

is at the dunrod Hill sssi and GCR site, inverclyde [Ns 

23 72] with excellent exposures of feldspar-phyric hawaiite 

lavas and aphyric mugearite lavas, often as composite 

flows. Aphyric basal parts of individual flows grade 



26 

sharply but uninterrupted into feldspar-phyric upper parts 

suggesting that they were emplaced in rapid succession as 

pulses of the same eruption (see stephenson in stephenson 

et al., 2003). 


From Cloch point [Ns 20 75] and dunrod Hill [Ns 24 

72] to port Glasgow [Ns 32 74] the strathgryfe lava 

member rests disconformably upon sedimentary rock 

of the underlying Clyde sandstone Formation. To the 

south and south-east of there, from loch Thom [Ns 25 

71] to largs [Ns 20 59], the strathgryfe lava member 

is conformably underlain by earlier lavas and tuffs of 

the Clyde plateau volcanic Formation. in that area the 

underlying Greeto lava member consists dominantly 

of flows of plagioclase-microphyric basalt (‘Jedburgh’ 

type). To the south, in the Kilbirnie Hills, the strathgryfe 

lava member extends southwards beyond the limit of 

the Greeto lavas and rests unconformably on the late 

devonian Kelly Burn sandstone Formation, stratheden 

Group (Browne et al., 2001). 

in the Renfrewshire Hills, the dominantly olivine-free 

lavas (mugearite and hawaiite) of the upper part of the 

strathgryfe lava member are overlain by the more-mafic 

olivine-bearing basalts (‘dunsapie’ and ‘Craiglockhart’ 

types) of the marshall moor lava member. The change is 

abrupt and could imply a significant time interval between 

the two volcanic episodes. To the south, on the southeastern 

edge of the Kilbirnie Hills, the thinning strathgryfe 

lava member is overlain directly by the volcaniclastic 

Kirkwood Formation and the lower limestone Formation. 

To the south of the muirshiel Fault, upper and lower parts 

to the strathgryfe lava member have been informally identified 

(paterson et al., 1990). in this area the strathgryfe 

lava member is separated by the lavas and volcaniclastic 

deposits of the misty law Trachytic member (paterson et 

al., 1990). 

Thickness 

The member is estimated to be up to 750 m thick in the 

northern and central part of of the Renfrewshire Hills 

(paterson et al., 1990, table 6) and up to 250 m thick in the 

Kilbirnie Hills (monro, 1999, p. 32). 


The member occurs in the northern and central parts of 

the Renfrewshire Hills from Greenock [Ns 28 76] to the 

muirshiel Fault [Ns 23 65] to east Queenside muir [Ns 31 

65] and underlies the length of the valley of the Gryfe water. 

south of the muirshiel Fault, the strathgryfe lava member 

underlies the River Calder valley [Ns 31 64 to 35 60] and 

ladyland moor [Ns 30 59]. in this region the member has 

been informally split into upper and lower parts (paterson 

et al.,1990) separated by the misty law Trachytic member. 

The unit extends south into the Kilbirnie Hills but thins 

markedly south and into the area of the Busbie muir [Ns 24 

46] and munnoch [Ns 25 47] reservoirs. it is represented by 

only a few flows where it is cut out by the extension of the 

paisley Ruck fault system [around Ns 25 44]. 

Age 


4.3.3.6 MarsHall Moor lava MeMBer 

Name 

previously named the marshall moor lavas (paterson et 

al., 1990). part of the ‘lower Group’ of Richey (1928) and 

‘unit 4’ of Johnstone (1965). see also monro (1999).

Lithology 

macroporphyritic mafic basalts; olivine-clinopyroxeneplagioclase-macrophyric 

basalt (‘dunsapie’ type) and 

olivine-bearing plagioclase-macrophyric basalt (‘markle’ 

type) with some olivine-pyroxene macrophyric basalt 

(‘Craiglockhart’ type or ‘ankaramite’). 

Stratotype 

The type area includes the thickest part of the unit between 

peockstone [Ns 357 610] and Bridge of weir [Ns 388 655] 

(see paterson et al., 1990). 


lavas of the marshall moor lava member are considerably 

more mafic than those of the underlying strathgryfe lava 

member. The abrupt change may imply a significant time 

interval between the two petrologically distinct volcanic 

episodes. 

A marked petrographical change distinguishes the macroporphyric 

mafic basalts (‘dunsapie’ and ‘Craiglockhart’ 

types) of the marshall moor lava member from the overlying 

microporphyric mafic basalts (mainly ‘dalmeny’ type) 

of the Kilbarchan lava member. 

Thickness 

up to 75 m 


in the south-eastern Renfrewshire Hills: the thickest 

development of the member occurs in the area between 

peockstone [Ns 357 610] and Bridge of weir [Ns 388 655] 

and it is well exposed around marshall moor [Ns 375 625]. 

To the north it becomes discontinuous in faulted outcrops 

between yonderton [Ns 390 667] and Barochan [Ns 420 

693]. To the south, outliers occur around lochwinnoch golf 

course [Ns 344 597] and a single flow occurs beneath the 

Kilbarchan lava member between Glenlora and the maich 

water [Ns 324 587]. The most southerly outcrops are on 

the east side of the maich water around ladyland [Ns 325 

578]. 

Age 


4.3.3.7 KilBarCHan lava MeMBer 

Name 

previously named the Kilbarchan lavas (paterson et al., 

1990). part of the ‘lower Group’ of Richey (1928) and 

‘unit 5’ of Johnstone (1965). 

Lithology 

microporphyritic mafic basalts; olivine-microphyric basalt 

(‘dalmeny’ type) with rare flows of clinopyroxene-olivinemicrophyric 

basalt (‘Hillhouse’ type). Around Castle 

semple and at Gladstone (see below) a few isolated flows 

of olivine-pyroxene-macrophyric basalt (‘ankaramite’ or 

‘Craiglockhart’ type) occur. 

Stratotype 

The unit crops out over a wide type area between Castle 

semple loch [Ns 360 595] and Ranfurly [Ns 395 650] (see 

paterson et al., 1990). 


At the lower boundary, a marked petrographical change 

occurs from macroporphyric mafic basalts (‘dunsapie’ 

and ‘Craiglockhart’ types) of the underlying marshall 

moor lava member to the microporphyric mafic basalts 

27 

(mainly ‘dalmeny’ type) of the overlying Kilbarchan lava 

member. 

The Kilbarchan lava member is overlain across an erosional 

boundary by volcaniclastic sedimentary rocks of the 

Kirkwood Formation, which contain detrital material from 

the underlying lavas. 

Thickness 

up to 75 m 


The member crops out over a wide area in the Renfrewshire 

and Beith–Barrhead hills, between Castle semple loch [Ns 

36 59] and Ranfurly [Ns 39 65] and extends east to the 

town of Kilbarchan [Ns 40 63]. it continues northwards, 

somewhat thinned, to Barochan [Ns 410 690] where the 

outcrop is terminated by a system of major east-north-east- 

and west-north-west-trending faults. in the south, outcrops 

of the Kilbarchan lava member are terminated by a major 

east–west fault system at lochwinnoch [Ns 36 59], but 

thin outliers occur at the top of the lava succession between 

Glenlora [Ns 324 587] and south of ladyland [Ns 325 

575]. 

Age 


BEITH–BARRHEAD HILLS 

4.3.3.8 glenBurn volCaniClasTiC MeMBer (gBv) 

Name 

Named from Glen park, paisley. The Glenburn 

volcaniclastic member, which appears on current printed 

BGs publications, including the Glasgow district memoir 

and bedrock geology map, was defined and recorded as 

the now obsolete Glenburn volcanic detrital member by 

iGs (1981). it also replaces the now obsolete Glen park 

volcanic detrital member. see Hall et al. (1998). 

Lithology 

The Glenburn volcaniclastic member comprises 

interbedded purplish red medium-grained sandstone, with 

subordinate reddish purple silty mudstone and reddish 

purple muddy siltstone. some of the sandstone grains 

are described as volcaniclastic. in the Glenburn Borehole 

(BGs Registration Number Ns46se/164) [Ns 4783 6065] 

volcaniclastic sedimentary rocks and agglomerates are 

interbedded with several (thin) lava flows. 

Stratotype 

The type section is the Glenburn Borehole (see above) from 

17.35 to 43.54 m depth, where volcaniclastic sedimentary 

rocks and agglomerates are interbedded with several (thin) 

lava flows. A partial type section occurs in the bed of the 

Craigie linn [Ns 4743 6047 to 4744 6053] within Glen 

park, paisley. 


The lower boundary of the member is seen in the Glenburn 

Borehole (see above) at 43.54 m depth (iGs, 1981). it is 

sharp, faulted and marked by a lithological change from the 

red-brown sedimentary rocks of the Kinneswood Formation 

(inverclyde Group) to basalt lavas (‘markle’ and mugearite 

types). 

The upper boundary is exposed and clearly seen at 

Craigie linn waterfall [Ns 475 605] in Glen park, paisley. 

The top of the member is sharp and marked by a lithological 

change from well-bedded purple tuffs and volcaniclas- 



tic sedimentary rocks to grey plagioclase-microphyric 

basalt lava (‘Jedburgh’ type) of the overlying Gleniffer 

lava member (Clyde plateau volcanic Formation). 

elsewhere the unit is overlain by the distinctive olivinebearing 

plagioclase-macrophyric basalts (‘markle’ type) 

that are most characteristic of this overlying member. The 

top of the member is also seen in the Glenburn Borehole 

(see above) at 17.59 m depth (iGs, 1981) where white 

to grey sandstone with slump structures is overlain by 

agglomerate of the Gleniffer lava member (Clyde plateau 

volcanic Formation) that comprises subangular clasts of 

yellowish sandstone and basalt in a fine-grained purplish 

grey matrix. 

Thickness 

The thickness is variable from over 26 m in the Glenburn 

Borehole, to more than 30 m at outcrop in Glen park (see 

above). 


The Glenburn volcaniclastic member is exposed at intervals 

along the base of the lava scarp from Craigie linn [Ns 475 

605] to Harelaw Burn [Ns 49 60] including the Glen park, 

paisley. 

Age 


4.3.3.9 gleniFFer lava MeMBer 

Name 

previously known as the ‘Gleniffer lavas’ (Hall et al., 

1998, monro, 1999; paterson et al., 1990), ‘lower Group 

(a)’ (Richey et al., 1930). 

Lithology 

The member comprises distinctive olivine-bearing 

plagioclase-macrophyric basalts (‘markle’ type). 

Characterised by lavas with abundant, platy phenocrysts of 

plagioclase up to 25 mm long and microphenocrysts of redbrown 

olivine. A massive flow of plagioclase-microphyric 

basalt (‘Jedburgh’ type) forms the base of the member at 

linn well [Ns 475 605]. The lavas are interbedded with 

volcaniclastic sedimentary rocks at the base. 

Stratotype 

The Gleniffer lava member crops out in a prominent scarp 

in its type area along the north side of Gleniffer Braes to 

Brownside Braes [Ns 450 607 to 485 605] (see Hall et al., 

1998). 


The Gleniffer lava member is underlain by the sedimentary 

rocks of the Glenburn volcaniclastic member to the north 

and east of Brownside Braes [Ns 485 605]. 

The member is overlain and may be cut out or overlapped, 

by the mafic basalts of the sergeantlaw lava 

member around sergeantlaw [Ns 455 597] and to the east 

of middleton [Ns 445 579], and to the west of Barcraigs 

Reservoir [Ns 39 57] and walls Hill [Ns 41 59]. 

Thickness 

The thickness is not stated. 


The Gleniffer lava member crops out in the Beith–Barrhead 

Hills to the east of Barcraigs Reservoir [Ns 39 57] and is 



28 

faulted against the Kirkwood Formation and lawmuir 

Formation in the north, to the north of High Burnside [Ns 

42 60]. it extends eastwards through Gleniffer Braes [Ns 

450 607] to Brownside Braes [Ns 485 605]. To the south 

the unit is faulted against the upper limestone Formation 

in loch libo [Ns 435 556], and the limestone Coal 

Formation by the dusk water Fault. 

Age 


4.3.3.10 sergeanTlaw lava MeMBer 

Name 

previously known as the ‘sergeantlaw lavas’ (Hall et al., 

1998; monro, 1999; paterson et al., 1990), ‘lower Group 

(b)’ (Richey et al., 1930). 

Lithology 

olivine-microphyric basalt (‘dalmeny’ type) and olivineclinopyroxene-plagioclase-macrophyric 

basalt (‘dunsapie’ 

type). in the closure of the Beith Anticline the basal flow 

of the member is a distinctive clinopyroxene-olivinemacrophyric 

basalt (‘ankaramite’ or ‘Craiglockhart’ type). 

in Boylestone Quarry [Ns 495 597] hydrothermal veins and 

cavities contain a wide variety of minerals including calcite, 

analcime, prehnite, heulandite, bowlingite, thomsonite and 

natrolite. Native copper, cuprite and malachite are also 

found. 

Stratotype 

The sergeantlaw lava member is well seen in its type area 

between sergeantlaw [Ns 455 596] and Greenfieldmuir 

[Ns 456 583] (Hall et al., 1998). Also between Townhead 

of Threepwood [Ns 39 55] and Gillies Hill [Ns 38 54] (see 

monro, 1999). 


The sergeantlaw lava member overlies the plagioclasemacrophyric 

basalts (‘markle’ type) of the Gleniffer lava 

member. south of wester Gavin [Ns 380 589] the mafic 

basalts of the sergeantlaw lava member appears to rest 

upon volcaniclastic sedimentary rocks and it is possible that 

in this area the underlying Gleniffer lava member has been 

overlapped. To the north of Harelaw Reservoir [Ns 485 

590] the sergeantlaw lava member appears to cut out or 

overlap most of the Gleniffer lava member. 

Resting upon the sergeantlaw lava member and 

forming a broad dip slope outcrop south of muirdykes 

[Ns 395 591] are the plagioclase-macrophyric basalts 

(‘markle’ type) and olivine-clinopyroxene-plagioclase 

macrophyric basalts (‘dunsapie’ type) of the Fereneze 

lava member. 

Thickness 

Not stated. 


The Renfrewshire and Beith–Barrhead hills: the sergeantlaw 

lava member crops out to the north and south of Barcraigs 

Reservoir [Ns 39 57]. it is well seen between Townhead 

of Threepwood [Ns 39 55] and Gillies Hill [Ns 38 54] and 

forms scarp features around walls Hill [Ns 412 589]. it is 

also present in the area between sergeant law [Ns 455 596] 

and Greenfieldmuir [Ns 456 583] and in the lochliboside 

Hills [Ns 450 575]. 

Age 

mid visean (Arundian to Asbian).

4.3.3.11 Ferenze lava MeMBer 

Name 

previously known as the ‘Fereneze lavas’ (Hall et al., 

1998; monro, 1999; paterson et al., 1990) and equated with 

‘lower Group (c)’ (Richey et al., 1930). 

Lithology 

mainly plagioclase-macrophyric basalt (‘markle’ type) 

and olivine-clinopyroxene-plagioclase macrophyric basalts 

(‘dunsapie’ type). several flows of mugearite are present, 

two were encountered in a borehole at Crummock park 

[Ns 350 540], Beith and three in loanhead Quarry [Ns 365 

555] where a discontinuous bed of tuff is also seen. These 

flows are 15 m, 8 m and over 10 m thick and are separated 

by boles up to 0.5 m thick. The basalts are amygdaloidal 

with much hydrothermal alteration giving a range of 

secondary minerals such as calcite, prehnite, analcime, 

thomsonite, natrolite, bowlingite and heulandite. The quarry 

is well known for copper mineralisation with native copper, 

malachite and cuprite recorded. 

Stratotype 

The best exposure of the Fereneze lava member is in its 

type area on the north-west limb of the Beith Anticline, 

to the west of Barcraigs Reservoir [Ns 38 57]. Here flows 

of mainly olivine-basalts form good scarp and dip slope 

topography (‘trap features’). A reference section is the 

Crummock park Borehole [Ns 350 540] which penetrated 

120 m of the Fereneze lava member, but no detailed 

geological log is available (see monro, 1999). 


The ‘markle’ and ‘dunsapie’ basalts of the Fereneze lava 

member appear to cut or overlap most of the underlying 

‘dalmeny’ and ‘dunsapie’ basalts of the sergeantlaw lava 

member in the area of the Fereneze Hills. 

in the west of the Beith–Barrhead Hills, Bog Hall [Ns 

362 540] to Newton of Belltrees [Ns 372 582], the Fereneze 

lava member is overlain by the olivine-microphyric basalts 

(‘dalmeny’ type) of the Beith lava member. The upper boundary 

of the unit is not seen in the eastern Beith–Barrhead Hills. 

Thickness 

The maximum thickness is greater than 120 m. 


North-west limb of the Beith Anticline, to the west of 

Barcraigs Reservoir [Ns 384 570] where the member 

forms good scarp and dip slope topography. it is faulted 

out in the south against the Blackhall limestone and lower 

limestone Formation (Clackmannan Group) by the dusk 

water Fault to the south of Blaelochhead [Ns 395 532]. in 

the east (south-east limb of the Beith anticline), the member 

underlies the Fereneze Hills between Capellie Farm [Ns 

465 583] and the top of Boylestone Quarry [Ns 495 597]. 

Age 


4.3.3.12 BeiTH lava MeMBer 

Name 

The Beith lava member was previously known as the 

‘Beith lavas’ (paterson et al. 1990; monro 1999), and the 

‘upper Group’ (Richey et al. 1930). 

Lithology 

The formation comprises olivine-microphyric basalt 

(‘dalmeny’ type). Red boles are common between 

29 

flows and interbedded chocolate-coloured ‘marls’ are 

present. evidence from outcrop and the Crummock park 

borehole [Ns 3503 5392] suggests large parts of the 

flows are extensively altered and decomposed. south 

of Roebank Glen [Ns 353 554] a flow of plagioclasemacrophyric 

basalt (‘markle’ type) crops out within the 

member. 

Stratotype 

The Beith lava member crops out in its type area on lower 

slopes at the south-west limit of the Beith–Barrhead Hills 

between [Ns 35 54] and [Ns 36 57] (see monro, 1999). 

A reference section is the Crummock park Borehole (see 

above) which penetrates the lowest 50 m of the Beith lava 

member, but no detailed geological log is available (see 

monro, 1999). 


The member is underlain by the ‘markle’ and ‘dunsapie’ 

-type basalts of the Fereneze lava member. 

The member is overlain by volcaniclastic sedimentary 

rocks of the Kirkwood Formation (strathclyde Group) 

wherever the top of the member crops out. 

Thickness 

About 90 m 


The member occurs to the west and south-west of the 

Beith–Barrhead Hills, on the north-west limb of the Beith 

Anticline, but is faulted out on the south-eastern limb. The 

unit underlies the town of Beith [Ns 35 54] and extends 

north-east until it is faulted out against the paisley Ruck 

Fault just north of east Gavin [Ns 389 599]. 

Age 


DUNLOP–EAGLESHAM BLOCK 

4.3.3.13 lower Flow Moss lava MeMBer 

Name 

previously known as the Flow moss lavas (lower). see 

macpherson and phillips (1997); phillips and macpherson 

(1996); macpherson et al. (2000). 

Lithology 

The lower Flow moss lava member consists of alkali 

basalt and subordinate basanite. 

Stratotype 

The type area is the dunlop–eaglesham moors between 

Glasgow, Kilmarnock and Hamilton, limited to the 

southern part of the area between stewarton [Ns 4200 

4500] in the west and Craufurdland water [Ns 510 448] 

in the east. 


The nature of the base is unknown but may be unconformable 

on the inverclyde Group or older strata. 

The member is overlain by and interbedded with the 

moyne moor lava member in the western part of the 

area of occurrence. elsewhere, where locally known, a 

thick bole is developed on the uppermost flow at [Ns 

510 448] and the upper Flow moss lava member rests 

on this. 

Thickness 

Not stated 




dunlop–eaglesham moors between Glasgow, Kilmarnock 

and Hamilton, limited to the south of the area between 

stewarton [Ns 4200 4500] in the west and Craufurdland 

water [Ns 510 448] in the east. 

Age 


4.3.3.14 Moyne Moor lava MeMBer 

Name 

previously named the moyne moor lavas. see macpherson 

and phillips (1997); phillips and macpherson (1996); 

macpherson et al. (2000). 

Lithology 

The moyne moor lava member consists of plagioclasephyric 

trachybasalt (hawaiite) with discrete subordinate 

alkali basalt and rare basaltic-trachyandesite (mugearite) 

near the top of the member. These may represent the 

initiation of the more evolved trachytic volcanism of the 

overlying Harelaw lava member. 

Stratotype 


Glasgow, Kilmarnock and Hamilton, irregularly shaped, 

but in continuous outcrop from Balgray Reservoir [Ns 5100 

5700] to over Auchentibber Farm [Ns 4560 4980]. 


The member rests upon and is interbedded with the lower 

Flow moss lava member in the south but elsewhere its 

base is possibly unconformable on the sedimentary strata of 

the Ballagan Formation (inverclyde Group) but the contact 

is not seen due to faulting. 

The member is overlain by the geographically separate 

(and laterally equivalent) alkali basalts of the eaglesham 

and Neilston lava members and the trachytic Harelaw lava 

member. The contacts are considered conformable, but may 

also be locally unconformable. 

Thickness 

more than 100 m 



and Hamilton, irregularly shaped, but continuous 

outcrop from Balgray Reservoir [Ns 5100 5700] to over 

Auchentibber Farm [Ns 4560 4980]. 

Age 


4.3.3.15 neilsTone lava MeMBer (nnla) 

Name 

previously named the Neilston lavas. see macpherson 



Lithology 

The Neilston lava member consists of alkali basalts with 

minor basanite in the lower part and trachybasalt in the 

upper. 

Stratotype 


Glasgow, Kilmarnock and Hamilton, in the western part of 



30 

the area between Neilston [Ns 4800 5700] and stewarton 

[Ns 4300 4800]. 


The base is apparently conformable (though it may locally 

be unconformable) on the moyne moor lava member, 

which consists predominantly of trachybasalt. 

The member is overlain by the trachytic Harelaw lava 

member. The contact is unconformable. 

Thickness 

more than 100 m. 



and Hamilton, in the western part of the area between 

Neilston [Ns 4800 5700] and stewarton [Ns 4300 4800]. 

Age 


4.3.3.16 Darvel lava MeMBer 

Name 

previously named the darvel lavas. see macpherson 



Lithology 

The darvel lava member consists of alkali basalts and 

basanites. Near the unit top, trachybasalt also occurs. 

Stratotype 


Glasgow, Kilmarnock and Hamilton, limited to around 

darvel [Ns 6000 4000] and Newmilns [Ns 5000 3700] just 

north of the inchgottrick Fault. 


The darvel lava member is unconformable on the mainly 

lithic arenite succession of the lower devonian swanshaw 

sandstone Formation (see Browne et al., 2002). 

The member is mainly overlain by the Kirkwood 

Formation of the strathclyde Group. The contact is considered 

unconformable with the volcaniclastic sedimentary 

rocks draping an eroded land surface formed from the member. 

locally, the member is interbedded with, or overlain 

by, the Gowk stane volcaniclastic member. 

Thickness 

Not known 


dunlop–eaglesham moors between Glasgow, Kilmarnock and 

Hamilton, limited in area around darvel [Ns 6000 4000] and 

Newmilns [Ns 5000 3700] just north of the inchgottrick Fault. 

Age 


4.3.3.17 DuMDruFF Hill lava MeMBer (DHla) 

Name 

previously named the dumdruff Hill lavas. see macpherson 



Lithology 

The dumdruff Hill lava member consists of trachyandesite 

and trachytic lava.

Stratotype 


Glasgow, Kilmarnock and Hamilton, around Ballageich 

[Ns 5200 5200] and Braidley moss [Ns 6100 4100] south 

of dumdruff Hill. 


The base is unconformable on the eaglesham lava member 

that consists of basaltic lavas. 

The member is overlain in part by the Gowk stane 

volcaniclastic member and the Harelaw lava member, 

with which it is partly interbedded. The upper Flow moss 

lava member also rests on this member locally. 

Thickness 

Between 45 and 70 m 



and Hamilton around Ballageich [Ns 5200 5200] and 

Braidley moss [Ns 6100 4100] south of dumdruff Hill. 

Age 


4.3.3.18 Harelaw lava MeMBer 

Name 

previously named the Harelaw lavas. see macpherson 



Lithology 

The Harelaw lava member consists of trachyte, 

trachyandesite and trachybasalt lava. 

Stratotype 


Glasgow, Kilmarnock and Hamilton, discontinous across 

an area around Halker [Ns 4100 5000], Neilston [Ns 5200 

5800], Glenouther Rig [Ns 4800 4800] and Blackwood Hill 

[Ns 5500 4700]. 


The base is unconformable on the moyne moor and 

Neilston lava members that consist of basaltic lavas. 

The member is overlain by the upper Flow moss lava 

member. The contact is considered unconformable and 

locally intrusive. The trachytic lava flows are thought to 

have had significant dome-like topographical expression 

immediately after eruption. 

Thickness 




and Hamilton, discontinous across an area around Halker 

[Ns 4100 5000], Neilston [Ns 5200 5800], Glenouther Rig 

[Ns 4800 4800] and Blackwood Hill [Ns 5500 4700]. 

Age 


4.3.3.19 eaglesHaM lava MeMBer 

Name 

previously named the eaglesham lavas. see macpherson 



31 

Lithology 

The eaglesham lava member is dominated by alkali basalt, 

but also includes basanite and feldspar-phyric trachybasalt. 

one trachytic flow is known. 

Stratotype 


Glasgow, Kilmarnock and Hamilton, in the eastern part 

of the area between Newton mearns [Ns 5750 5180] and 

eaglesham [Ns 5360 5570]. 


The base is apparently conformable on the moyne moor 

lava member that consists predominantly of trachybasalt 

but may locally be unconformable. 

The member is overlain by the dumdruff Hill lava 

member. The contact is considered conformable. 

Thickness 

up to 250 m 



and Hamilton, in the eastern part of the area between 

Newton mearns [Ns 5750 5180] and eaglesham [Ns 5360 

5570]. 

Age 


4.3.3.20 gowK sTane volCaniClasTiC MeMBer (gowK) 

Name 

The definition was published by macpherson and phillips 

(1997) and macpherson et al. (2000). see also macpherson 

and phillips (1998). 

Lithology 

mixed sequence of pyroclastic rocks and volcaniclastic 

sedimentary rocks, which are locally derived and mainly 

trachytic in composition (macpherson and phillips, 1997). 

There is a marked lateral variation in deposits within the 

Gowk stane volcaniclastic member. in the northern part 

of the outcrop, south of eaglesham [Ns 570 520] to the 

vicinity of Carrot Farm [Ns 575 481], and north-east of 

darvel the member consists of primary pyroclastic rocks 

with limited reworking. These include rocks of trachytic 

and basaltic composition. The pyroclastic rocks are poorly 

sorted, grey to grey-green, lapilli-tuff and/or agglomerate. 

Beds are generally less than 0.5 m thick and exhibit 

normal grading, either within the lapilli-tuff matrix or in 

the distribution of blocks in typically matrix-supported 

agglomerate. in the southern part of the outcrop, such as 

that exposed in Glen water [Ns 587 432 to 579 413], 

the Gowk stane volcaniclastic member is dominated by 

volcaniclastic sedimentary rocks (macpherson and phillips, 

1997). This thickly bedded sedimentary sequence consists 

of interbedded mudstone, siltstone and tuffaceous sandstone 

with sporadic conglomerate units. The mudstones and 

siltstones are pinkish brown, the sandstones are greenish 

grey to buff coloured and poorly to locally well sorted with 

fragments of volcanic rock. 


in the northern part of the outcrop (see above) and north-east 

of darvel, the member is dominated by primary pyroclastic 

deposition, but in the south (see above), fluviatile processes 

dominated. Here the volcaniclastic sedimentary rocks, 

locally derived by penecontemporaneous weathering and 



erosion of the pyroclastic deposits and lavas, include 

channel and chaotic mass movement (lahar-type) deposits 

(see macpherson and phillips, 1997). 

Stratotype 

The type section comprises exposures at [Ns 5692 5092] of 

pyroclastic strata on an approximately 20 m high, partially 

grassed, north-facing slope, and in a small, disused quarry 

at the crest of the slope 600 m north of east Revoch Farm 

[Ns 569 508], 1.2 km south-south-west of eaglesham, 

east Renfrewshire (macpherson and phillips, 1998). A 

partial type section includes exposures of volcaniclastic 

strata in the Glen water river valley, near laigh overmuir 

Farm, 6 km north-north-east of darvel, strathclyde [Ns 

5790 4140 to 5860 4320] (macpherson and phillips, 1997; 

macpherson et al., 2000). 


The pyroclastic and volcaniclastic strata of the Gowk 

stane volcaniclastic member are inferred to overlie and be 

penecontemporaneous with the eaglesham and dumdruff 

Hill lava members within the Clyde plateau volcanic 

Formation (macpherson and phillips, 1997; macpherson 

et al., 2000). volcaniclastic sedimentary breccia and 

pyroclastic breccia of the Gowk stane volcaniclastic 

member appear directly to overlie trachyandesite of the 

dumdruff Hill lava member at east Revoch Farm [Ns 569 

508] although the contact is not exposed (macpherson and 

phillips, 1998). 

The upper boundary of the Gowk stane volcaniclastic 

member is not seen, but is inferred to be overlain by 

the upper Flow moss lava member, within the Clyde 

plateau volcanic Formation (macpherson and phillips, 

1997; macpherson et al., 2000). 

Thickness 

Based on the vertical section on 1:10 000 scale Geological 

sheet Ns54se (whitelee Forest), the minimum thickness 

is 60 m. 


The type area is in the dunlop–eaglesham moors between 

Glasgow, Kilmarnock and Hamilton, specifically between 

eaglesham [Ns 570 520] and darvel [Ns 565 375]. 

Age 


4.3.3.21 uPPer Flow Moss lava MeMBer 

Name 

previously known as the Flow moss lavas (upper). see 

macpherson and phillips (1997); phillips and macpherson 

(1996); macpherson et al. (2000). 

Lithology 

The upper Flow moss lava member consists of alkali 

basalts and subordinate basanites and ‘ankaramites’. 

Stratotype 


Glasgow, Kilmarnock and Hamilton, limited to the southern 

part of the area between Craufurdland water [Ns 510 448] in 

the north-west and darvel [Ns 6100 3900] in the south-east. 


The base is apparently unconformable on the Harelaw 

lava member that consists of trachytic lavas and the 

volcaniclastic rocks of the Gowk stane volcaniclastic 



32 

member. A thick bole formed on the top flow of the lower 

Flow moss lava member at [Ns 510 448] marks the 

contact with this underlying member. 

The member is overlain unconformably by the Kirkwood 

Formation (strathclyde Group). 

Thickness 

Not stated 



and Hamilton, limited to the southern part of the area 

between Craufurdland water [Ns 510 448] in the northwest 

and darvel [Ns 6100 3900] in the south-east. 

Age 


KILPATRICK HILLS 

4.3.3.22 BurnCrooKs volCaniClasTiC MeMBer 

Name 

previously known as the Burncrooks pyroclastic member 

(Hall et al., 1998). 

Lithology 

volcaniclastic sedimentary rocks, some lacustrine, tuff 

and agglomerate. pyroclastic rocks include cones which 

in some places coalesce. lacustrine sedimentary rocks in 

the form of mudstone containing fish scales, overlying a 

discontinuous coal seam, are exposed south of Rigangower 

[Ns 438 757]. 

Stratotype 

The member crops out around Fyn loch [Ns 460 772] 

and lily loch [Ns 473 780] where it is 10–20 m thick 

and consists mainly of tuff and volcaniclastic sedimentary 

rocks. A reference section is the loch Humphrey Borehole 

(BGs Registration Number Ns47Ne/1) [Ns 4582 7555] 

that penetrates the entire 70 m thickness of the Burncrooks 

volcaniclastic member, which is overlain by the Auchineden 

lava member and underlain by sedimentary rocks of the 

Clyde sandstone Formation. in the borehole, the member 

mainly consists of tuff and lapilli-tuff, with a few thin lavas 

and sandstone beds. A full geological description of the 

core is available. 


The Burncrooks volcaniclastic member is underlain by 

the sedimentary rocks of the Clyde sandstone Formation 

(inverclyde Group). 

The member is overlain by the lavas of the Auchineden 

lava member and saughen Braes lava member. 

Thickness 

Between 0 and 80 m, very variable, thins to the north-east 

and south. 


The Burncrooks volcaniclastic member crops out along the 

north-western and western margins of the Kilpatrick Hills 

lava block. it stretches from north-east of Bowling [Ns 

455 739] to Burncrooks Reservoir [Ns 482 796] with more 

isolated patches along the northern margin of the faulted 

block as far east as [Ns 5500 8000]. 

Age 

mid visean (Arundian to Asbian).

4.3.3.23 saugHen Braes lava MeMBer 

Name 

previously named the saughen Braes lavas (Hall et al., 

1998). 

Lithology 

plagioclase-macrophyric basalts (‘markle’ type). 

Stratotype 

The unit crops out in its type area on saughen Braes [Ns 

462 783], where it consists of about five flows. 


The saughen Braes lava member interdigitates with the 

Auchineden lava member and in places underlies it, for 

example around Black linn Reservoir [Ns 443 772]. To 

the west of lang Craigs [Ns 430 760] the sequence is only 

represented by the Auchineden lava member. where the 

saughen Braes lava member is fully developed to the 

north-east of the area, it is underlain by the Burncrooks 

volcaniclastic member. The saughen Braes lava member 

interdigitates with and is overlain by the Auchineden lava 

member. 

Thickness 



Kilpatrick Hills: the unit occurs on saughen Braes [Ns 462 

783], thinning out to the south near Fynloch [Ns 458 770]. 

Age 


4.3.3.24 auCHineDen lava MeMBer 

Name 

previously known as the Auchineden lavas (Hall et al., 

1998). 

Lithology 

The member comprises plagioclase-microphyric basalts 

(‘Jedburgh’ type), with some mugearites and interbedded 

cone-facies tuffs. on the langs Craigs [Ns 430 760] 

there is an olivine-clinopyroxene-macrophyric basanite lava 

(‘Craiglockhart’ type). 

Stratotype 

The member is well exposed in its type area on the west 

flank of Auchineden Hill [Ns 493 805]. A reference section 

was encountered in the loch Humphrey Borehole (BGs 

Registration Number Ns47Ne/1) [Ns 4582 7555]. Here it 

is 45 m thick and lies below the Carbeth lava member and 

above the Burncrooks volcaniclastic member. it consists 

of mainly aphyric and microporphyritic lavas of ‘Jedburgh’ 

type with a flow of ‘markle’ type. A geological description 

of the core is available. 


in the area around saughen Braes [Ns 462 783] the 

Auchineden lava member is underlain by, and interdigitates 

with, the saughen Braes lava member. in the north and 

west of the Kilpatrick Hills the Auchineden lava member 

is directly underlain by the Burncrooks volcaniclastic 

member. The Auchineden lava member is overlain by the 

plagioclase-macrophyric lavas of the Carbeth lava member. 

Thickness 

Between 0 and 100 m, very variable. 

33 


Kilpatrick Hills: well exposed on the west flank of 

Auchineden Hill [Ns 493 805]. The Auchineden lava 

member thins out towards the north-east and is absent at 

Arlehaven [Ns 535 802]. west of Burncrooks [Ns 468 785] 

the member interdigitates with and overlies the saughen 

Braes lava member and becomes the only member present 

farther west on langs Craigs [Ns 430 760]. 

Age 


4.3.3.25 CarBeTH lava MeMBer 

Name 

previously named the Carbeth lavas (Hall et al., 1998). 

Lithology 

mainly plagioclase-macrophyric basalt (‘markle’ type). 

There are also some plagioclase-microphyric basalts 

(‘Jedburgh’ type) and olivine-clinopyroxene-plagioclasemacrophyric 

basalts (‘dunsapie’ type), as well as some 

mugearites near the base. 

Stratotype 

The lavas are well exposed in the type area around Carbeth 

[Ns 527 796] and in the scarps around the Birny Hills 

[Ns 495 770] (see Hall et al., 1998). A reference section 

was encountered in the loch Humphrey Borehole (BGs 

Registration Number Ns47Ne/1) [Ns 4582 7555] beneath 

the Greenside volcaniclastic member and above the 

Auchineden lava member. in the borehole, it is 20 m thick 

and consists of ‘markle’ type lavas with some ‘Jedburgh’ 

type and some thin beds of tuff. A geological log is available. 


The Carbeth lava member overlies the plagioclasemicrophyric 

basalts (‘Jedburgh’ type) of the Auchineden 

lava member. 

The member is unconformably overlain by the Greenside 

volcaniclastic member. west of loch Humphrey [Ns 455 

760] the member is reduced to one lava flow, which is 

preserved only in isolated patches below the volcaniclastic 

sedimentary rocks of the Greenside volcaniclastic member. 

Thickness 

Between 0 and 150 m. From the central part of the Kilpatrick 

Hills the member thins out towards the sw, partly due to 

erosion. it is some 80 m thick in the north-east of the region 

(Hall et al., 1998, table 5). 


The Carbeth lava member is geographically widespread in 

the Kilpatrick Hills, stretching from strath Blane [Ns 560 

790] in the north-east to Brown Hill [Ns 445 764] in the 

south-west. The member is well exposed around Carbeth 

and in the Birny Hills (see above). 

Age 


4.3.3.26 greensiDe volCaniClasTiC MeMBer 

Name 

The unit is known from outcrops in the area around 

Greenside Reservoir (see Hall et al., 1998). 

Lithology 

volcaniclastic sedimentary rocks, tuff and agglomerate, 

organic and clastic sedimentary rocks. west of Greenside, 



lacustrine mudstones containing fossil fish and wellpreserved 

plant remains and thin coal seams occur near the 

top of the member. 

Stratotype 

The unit is known from outcrops in its type area around 

Greenside Reservoir [Ns 475 755] (see Hall et al., 

1998). A reference section of the lower 21.35 m of the 

Greenside volcaniclastic member was penetrated by the 

loch Humphrey Borehole (BGs Registration Number 

Ns47Ne/1) [Ns 4582 7555] (from 0–21.35 m depth). in the 

borehole it consists mainly of tuff. 


The loch Humphrey Borehole (see above) penetrated the 

lowest 21.35 m of the Greenside volcaniclastic member, 

which overlies the lavas and pyroclastic rock of the Carbeth 

lava member. There is an unconformity between the two 

units and elsewhere the Greenside volcaniclastic member 

rests directly upon the Auchineden lava member. 

The Greenside volcaniclastic member is overlain by the 

lavas of the Cochno lava member. 

Thickness 

Between 0.5 and 55 m, but usually 5–10 m. Cones of pyroclastic 

rock at Clachan of Campsie [Ns 610 797] and Craigton [Ns 

525 770] cause the member to thicken to over 50 m. 


The Greenside volcaniclastic member (usually 5–10 m 

thick) forms a thin outcrop in the Kilpatrick Hills that runs 

north-east from Bowling [NN 454 370], through Greenside 

Reservoir [Ns 474 755] and High Craigton [Ns 525 766] to 

Blanefield [Ns 555 795]. The unit also crops out at the west 

end of loch Humphrey [Ns 451 762]. 

Age 


4.3.3.27 CoCHno lava MeMBer 

Name 

previously named the Cochno lavas (Hall et al., 1998). 

Lithology 

The Cochno lava member includes a wide range of lava 

types but is characterised by mafic varieties, particularly 

near the base. These include olivine-microphyric basalts 

(‘dalmeny’ type), olivine-clinopyroxene-macrophyric 

basalts (‘Craiglockhart’ type) and olivine-clinopyroxeneplagioclase-macrophyric 

basalts (‘dunsapie’ type). 

localised plagioclase-macrophyric basalts (‘markle’ type) 

and plagioclase-microphyric basalts (‘Jedburgh’ type) occur 

around Bowling [Ns 445 738]. 

Stratotype 

The Cochno lava member crops out in its type area between 

Cochno loch [Ns 500 760] and Craigton [Ns 520 770]. 


The Cochno lava member overlies the Greenside 

volcaniclastic member and represents the recommencement 

of lava extrusion after a major break in activity. it is overlain 

by the mugdock lava member. 

Thickness 

Between 100 and 250 m thick in the Kilpatrick Hills region. 

The member thins towards the north-east of the region, but 



34 

is thicker adjacent to the Campsie Fault (Hall et al., 1998, 

table 5). 


The Cochno lava member stretches north-east from 

Bowling [Ns 450 738] in the south-west of the Kilpatrick 

Hills to the south of Clachan of Campsie [NN 610 790] 

where the lavas are correlated with the Knowehead lava 

member of the western Campsie Fells area. Associated 

vents are located at Burnside [Ns 474 741], Black loch 

[Ns 500 765], and Craigton [Ns 525 770]. 

Age 


4.3.3.28 MugDoCK lava MeMBer 

Name 

previously named the mugdock lavas (Hall et al., 1998). 

Lithology 

predominantly plagioclase-macrophyric basalts 

(‘markle’ type). Near devil’s Craig dam [Ns 560 782] 

a few lavas have abundant feldspar phenocrysts of about 

5 mm and some up to 2 cm in length. Near Craigend 

Castle [Ns 548 777] a thin olivine-clinopyroxenemacrophyric 

basalt (‘Craiglockhart’ type) occurs and in 

the western part of the Kilpatrick Hills, mugearite lavas 

are present. 

Stratotype 

The mugdock lava member is well exposed in its type area 

between mugdock loch [Ns 554 773] and devil’s Craig 

dam [Ns 560 782]. 


The mugdock lava member overlies the more-mafic 

olivine-microphyric basalts (‘dalmeny’ type), olivineclinopyroxene-plagioclase-macrophyric 

basalts (‘dunsapie’ 

type) and olivine-clinopyroxene-macrophyric basalts 

(‘Craiglockhart’ type) of the underlying Cochno lava 

member. 

The mugdock lava member is overlain by the olivinemicrophyric 

basalts (‘dalmeny’ type) of the Tambowie 

lava member in the south of the Kilpatrick Hills. To 

the north, the Tambowie lava member is absent and the 

mugdock lava member is directly overlain by the sedimentary 

rocks of the lawmuir Formation (strathclyde Group). 

Thickness 

About 200 m thick in the north-east Kilpatrick Hills, 

thinning to about 100 m in the south-west of that area. 


Kilpatrick Hills. The mugdock lava member is present in 

the south of the area, between old Kilpatrick [Ns 465 730], 

where it is continuous with the upper part of the strathgryfe 

lava member of the Renfrewshire Hills lava block south 

of the River Clyde, and the area around mugdock [Ns 56 

77]. The lavas might have been derived from the waterhead 

volcano-complex in the Campsie Fells lava block. 

Age 


4.3.3.29 TaMBowie lava MeMBer 

Name 

previously named the Tambowie lavas (Hall et al., 

1998).

Lithology 

mainly olivine-microphyric basalt (‘dalmeny’ type) 

interbedded with mugearite. distal facies characteristics 

such as lava toes and thin reddened lavas with interbedded 

boles are well developed near edinbarnet [Ns 503 745]. 

The highest flow seen in the douglas muir area [Ns 525 

751] is an olivine-clinopyroxene-plagioclase-macrophyric 

basalt (‘dunsapie’ type) with an unusual cumulate texture. 

Stratotype 

The type area is the Kilpatrick Hills in limited extent 

between Tambowie [Ns 525 755] and muirhouses [Ns 506 

754]. 


The Tambowie lava member is underlain by the 

predominantly plagioclase-macrophyric basalts (‘markle’ 

type) of the mugdock lava member. 

The Tambowie lava member is the youngest unit in the 

Clyde plateau volcanic Formation of the Kilpatrick Hills. 

it is overlain by the sedimentary rocks of the lawmuir and 

Kirkwood formations (strathclyde Group). 

Thickness 

maximum 30 m 


only present in the southern part of the Kilpatrick Hills area, 

from east of Tambowie [Ns 525 755] west to muirhouses 

[Ns 506 754], and north of Cochno [Ns 497 745]. Absent 

from the north-east end of the Kilpatrick Hills around 

mugdock [Ns 56 77], and not present in the south-west 

of the Kilpatrick Hills area where it may be cut out by 

faulting. The lavas were possibly derived from the south or 

south-east. 

Age 


CAMPSIE BLOCK (Campsie Fells, Kilsyth Hills, Denny 

Muir) 

Note that there are local variations in the general 

stratigraphy as presented. This is related to the occurrence 

of interdigitation, the presence of unconformities, and the 

restricted distribution and multiple sources of some of the 

members. 

4.3.3.30 norTH CaMPsie PyroClasTiC MeMBer 

Name 

previously referred to informally as the North Campsie 

tephra deposits (BGs, 1993) and associated with the North 

Campsie linear vent system. 

Lithology 

The member consists of pyroclastic material deposited 

largely in tephra cones, as ashfall tuffs and lapilli tuffs and 

reworked volcaniclastic sedimentary rocks derived from 

the erosion of coallescing tephra cones. Typically, finely 

stratified tuffs pass upwards into coarse, unstratified spatter 

deposits and agglomerates. The lower agglomerates are 

composed largely of accidental and accessory material, 

including large blocks (up to 2 m) of basalt, variously 

weathered and textured smaller lava fragments and rare 

sandstone boulders. Higher agglomerates tend to be 

composed of essential tephra and scoria bombs in an upward 

progression that is typical of tephra cones. impersistent 

tongues and lenses of highly vesicular basaltic lava occur 

35 

locally. since fragmental rocks that form subaerial tephra 

cones are indistinguishable from those occupying necks, 

it is possible that some of the tephra is actually neck 

agglomerate (Craig, 1980). 

Stratotype 

Corrie of Balglass on the north side of the Campsie Fells 

[Ns 586 849 to Ns 595 854]. 2.5 km of cliffs, reaching a 

height of up to 200 m reveal an upward succession from 

tuffs and lapilli-tuffs with accidental and accessory clasts 

into agglomerates with an increasing proportion of essential 

scoria. large blocks (over 1 m) of dolerite are derived from 

the explosive brecciation of early-formed intrusions within 

the conduit system. impersistent tongues of scoriaceous 

lava increase in abundance upwards until the succession is 

composed largely of microporphyritic lavas but still with 

significant beds of pyroclastic rock (Craig, 1980). 


Rests unconformably on inverclyde Group strata of the 

Clyde sandstone Formation and overlain conformably or 

locally disconformably by the Campsie lava member of the 

Clyde plateau volcanic Formation. 

Thickness 

unspecified and probably highly variable. 


Continuous along lower parts of the northern escarpment of 

the Campsie Fells, from Canny Tops [Ns 551 833] in the 

west to Gonachan Cottage [Ns 629 860], on the south side 

of the endrick valley, in the east. Best exposures are in the 

type area around the Corrie of Balglass [Ns 586 849 to Ns 

595 854] and in precipitous cliffs on either side of the Black 

spout [Ns 610 863] and extending north-west towards 

dunmore [Ns 606 865]. 

Age 


4.3.3.31 DruMnessie lava MeMBer 

Name 

previously named the drumnessie lavas (see Forsyth et 

al., 1996). 

Lithology 

The drumnessie lava member consists of several lavas with 

intercalations, which make up to half the total thickness of 

the member, of agglomerate (including breadcrust bombs) 

and variably stratified lapilli-tuff. The lavas are mostly 

plagioclase-, plagioclase-olivine- and olivine-microphyric 

basalts (of ‘Jedburgh’ transitional to ‘dalmeny’ types), but 

there is also one clinopyroxene-olivine-macrophyric basalt 

(‘ankaramite’ of ‘Craiglockhart’ type). The latter forms 

the second lava in the Garrel Burn section [Ns 701 805], 

where the tuff and several lavas are well exposed. The 

lavas exhibit proximal characteristics. several nearby necks 

of the south Campsie linear vent-swarm are plugged by 

basalt of similar type (e.g. near st mirren’s well [Ns 721 

795]), and are probable sources of the lavas. 

Stratotype 

The type area is the south-central Kilsyth Hills, north-east 

of Glasgow [Ns 6954 7900 to 7414 8092] (Forsyth et 

al., 1996). A reference section is the BGs Tak-ma-doon 

Borehole (BGs Registration Number Ns78sw/5) [Ns 

7291 8053] in the south-central Kilsyth Hills, where a 43 m 



section penetrated the middle and basal lavas of the member 

(Craig, 1980). These notably included (in the upper part of 

the core) a 12.45 m-thick, vescicular, aphyric to plagioclasemicrophyric 

basalt, and a 6.47 m-thick, aphyric to olivinemicrophyric 

basalt, separated by more than 6 m of lapillituff. 

in the Banton Burn, the lower part of the member 

is exposed, upstream from the waterfall [Ns 731 804]. 

Three intensely jointed and locally scoriaceous plagioclasemicrophyric 

basalt lavas pass upwards into lapilli-tuff, 

before the sequence is truncated by the drumnessie Fault 

(Craig, 1980). To the north-east of the fault, there is a 

more-felsic flow, which forms a prominent feature below 

the topmost lapilli-tuff unit of the member, which is poorly 

exposed. 


The base is unconformable. in the BGs Tak-ma-doon 

borehole (see above) the basal lava of the drumnessie 

lava member was seen to overlie the Ballagan Formation, 

comprising 20 m of dominantly grey mudstone and siltstone, 

interbedded with many dolomitic cementstones, generally 

10–15 cm thick but ranging up to 0.5 m. However, 2 km to 

the west, in the Bachille Burn [Ns 707 793], the Ballagan 

Formation is absent, and the drumnessie lava member rests 

directly on the Kinnesswood Formation, which comprises 

sandstone and nodular limestone (cementstone). 

The drumnessie lava member is overlain conformably 

or disconformably by the laird’s loup lava member. The 

lithological change is to plagioclase-macrophyric basalt 

lava (‘markle’ type). 

Thickness 

up to 60 m. 


The member is restricted to the southern part of the Campsie 

Block (Forsyth et al., 1996) and specifically to the southern 

side of the central Kilsyth Hills, north-east of Glasgow. 

These rocks crop out to the north of the Campsie Fault, in 

faulted ground below the escarpment on the southern side 

of the Kilsyth Hills, north of Kilsyth, from east of Corrie 

[Ns 6954 7900], eastwards to beyond drumnessie [Ns 

7414 8092]. 

Age 


4.3.3.32 BurnHouse lava MeMBer 

Name 

previously named the Burnhouse lavas (see Forsyth et al., 

1996). 

Lithology 

The Burnhouse lava member consists mainly of thin 

(2–3 m-thick), ‘carbonated’ and relatively decomposed, 

heavily oxidised with much red veining, locally autobrecciated, 

plagioclase-macrophyric trachybasalt (hawaiite of ‘markle’ 

type) and a few thin intercalated plagioclase-microphyric 

trachybasalt lavas (hawaiite of ‘Jedburgh’ type) and 

intercalated tuff. The lavas have proximal facies characteristics, 

are irregular in form, and commonly amygdaloidal. To the 

north-east, along the southern shores of the Carron valley 

Reservoir [Ns 705 830], the plagioclase-macrophyric lavas 

are more massive and the plagioclase phenocrysts vary in 

size and concentration. The microporphyritic trachybasalt 

lavas are exposed on the southern slopes of Haugh Hill 

[Ns 680 832], in the Burnhouse area [Ns 688 823], and 

in the march Burn [Ns 709 830]. The associated tuffs are 



36 

also well exposed in the Burnhouse area and in the march 

Burn section where they comprise a series of well-stratified, 

red-weathered lapilli-tuffs and tuff-breccias with blocks and 

bombs, commonly up to 0.5 m in diameter and composed of 

various macroporphyritic and microporphyritic lava types. 

scoria and cementstone blocks are also incorporated within 

the tuffs, which are typically cut by numerous small faults 

and intruded by dykes. Two possible source necks have been 

identified at [Ns 682 825] and [Ns 708 824] on the basis of 

the coarseness of the tuffs (Craig, 1980). 

Stratotype 

The type area is the central Kilsyth Hills, north-east of 

Glasgow [Ns 6852 8196 to 7084 8316] (Forsyth et al., 

1996). A reference section is the Burnhouse Burn, central 

Kilsyth Hills, north-east of Glasgow [Ns 6897 8251 to 6850 

8199] (Craig, 1980). Here at [Ns 687 822] the tuffs are so 

coarse as to suggest the proximity of a source vent. The 

lavas are also well exposed at this locality, although they 

are subordinate to the tuffs. 


The basal plagioclase-macrophyric trachybasalt of the 

Burnhouse lava member is unconformable on sandstone 

of the underlying Clyde sandstone Formation (inverclyde 

Group). 

The Burnhouse lava member is overlain conformably, 

or disconformably, by the Campsie lava member. The 

change in lithology is to mainly plagioclase-microphyric 

basalt lavas (‘Jedburgh’ type). 

Thickness 

some 20 m. 


The member is restricted to the central part of the Campsie 

Block (Forsyth et al., 1996) and specifically to the central 

Kilsyth Hills, north-east of Glasgow. The largest area of 

outcrop is to the south-west of the Carron valley Reservoir, 

from Burnhouse Burn area [Ns 6852 8196] north towards 

Haugh Hill [Ns 6800 8357] and east to beyond the march 

Burn [Ns 7120 8304]. The other area of outcrop lies to the 

north of Garrel Hill [Ns 7036 8228 to 7122 8204]. 

Age 


4.3.3.33 lairD’s louP lava MeMBer 

Name 

previously named the laird’s loup lavas (Forsyth et al., 

1996). 

Lithology 

The laird’s loup lava member consists of plagioclasemacrophyric 

trachybasalt lavas of ‘markle’ type). individual 

lavas range in thickness from 6–15 m. The lavas are massive, 

and there is a lack of significant tuff between the lavas, 

suggesting that the flows are relatively distal. The lavas are 

variably altered and some are characterised by an ophitic 

texture. No specific source vent has been identified for the 

lavas, although the vent at Craigdouffie is a possible source 

(Craig, 1980), since the neck of the vent is infilled with 

breccia of similar material and exposures of the member 

near to the vent show proximal-facies characteristics. 

Stratotype 

The type area is the south-central Kilsyth Hills, north-east 

of Glasgow [Ns 6920 7974 to 7224 8068] (Forsyth et al.,

1996). A reference section, 50 m thick, occurs in the laird’s 

loup area of the Garrel Burn, south-central Kilsyth Hills 

[Ns 7032 8025 to 6992 8059] (Craig, 1980). Here, at least 

six lava flows are well exposed, and whilst the base of the 

member is not exposed, the topmost lava is. 


The basal trachybasalt of the laird’s loup lava member 

appears to be either conformable or disconformable on the 

underlying microporphyritic basalt lava of the drumnessie 

lava member. 

At the western end of its outcrop, the laird’s loup lava 

member is overlain by the Campsie lava member. The 

lithological change is to mostly plagioclase-microphyric 

basalt to trachybasalt (basalt to hawaiite of ‘Jedburgh’ 

type). At the eastern end of its outcrop, the member is overlain 

by the Tappetknowe lava member, the lithological 

change being to microporphyritic basaltic-trachyandesite 

(mugearite) and trachybasalt and rare plagioclase-macrophyric 

trachybasalt (‘markle’ type). 

Thickness 

some 65 m 





These rocks crop out along the escarpment on the southern 

side of the Kilsyth Hills, north of Kilsyth, from the southern 

flank of laird’s Hill [Ns 6920 7974], eastwards to Green 

Bank [Ns 7224 8068]. A further small area of outcrop in 

the Craigdouffie Burn [Ns 7424 8088 to 7437 8073] is 

tentatively correlated with the member. 

Age 


4.3.3.34 Carron BriDge lava MeMBer 

Name 

previously named the Carron Bridge lavas (see Forsyth et 

al., 1996). 

Lithology 

The Carron Bridge lava member consists predominantly 

of plagioclase-macrophyric trachybasalt lava (transitional 

from basalt to hawaiite of ‘markle’ type). The principal 

exposure of the member is in the River Carron, above and 

below the bridge [Ns 734 837 to 748 838], in the Faughlin 

area to the south [Ns 735 827], and near langhill [Ns 

775 844]. The lavas are relatively thick, some flows being 

in excess of 15 m, although in the langhill area, they are 

comparatively thinner, with about five lavas being present 

in the approximately 40 m-thick succession. All of the lavas 

are massive, moderately altered, and in the Carron Bridge 

and Faughlin areas, have particularly high concentrations 

of plagioclase phenocrysts, which tend to be elongate, up 

to 6 mm in length, and aligned in the presumed direction 

of flow. Fairly large pseudomorphed olivine phenocrysts 

are also present, but are less common than the plagioclase 

phenocrysts. Craig (1980) regarded these lavas as having 

distal-facies characterisitics. There is no indication of the 

source of the lavas. 

Stratotype 

The type area is in the eastern Kilsyth Hills, north-east of 


1996). A reference section is the River Carron, above and 

37 

below the bridge, north-west Kilsyth Hills, north-east of 

Glasgow [Ns 7348 8375 to 7480 8380] (Craig, 1980). 


The base has not been seen but is likely to be unconformable 

on sedimentary rocks of the inverclyde Group. 

in the section of the River Carron, below the bridge [Ns 

748 838], and in the Faughlin area to the south [Ns 735 

827], the Carron Bridge lava member is overlain, apparently 

conformably, or disconformably, by the Faughlin lava 

member. The lithological change is to tuff and agglomerate 

and basaltic-trachyandesite (mugearite). However, in the 

Carron River section above the bridge, and on its southern 

bank, the Faughlin lava member is absent, and the Carron 

Bridge lava member is overlain, disconformably or unconformably, 

by the Campsie lava member. 

Thickness 

more than 50 m, base not seen 


The member is restricted to the eastern part of the Campsie 

Block (Forsyth et al., 1996), specifically to the eastern 

Kilsyth Hills, north-east of Glasgow. These rocks crop out 

in inliers: in, and around, the Faughlin Burn [Ns 734 825] 

to [Ns 737 828]; in the River Carron [Ns 7348 8375 to 

748 838], and along the Faughlin Burn south to Faughlin 

Reservoir [Ns 7411 8295] and south-east to a locality at 

[Ns 7446 8248]; and east of langhill [Ns 7705 8300] to the 

River Carron [Ns 778 841], where the outcrop is truncated 

by the Carron Glen Fault (Craig, 1980). 

Age 


4.3.3.35 FaugHlin lava MeMBer 

Name 

previously named the Faughlin lavas (Forsyth et al., 1996). 

Lithology 

The Faughlin lava member, which is poorly exposed, 

consists predominantly of microphyric trachybasalt and 

basaltic-trachyandesite lava (hawaiite to mugearite). A 

single plagioclase-macrophyric trachybasalt (hawaiite of 

‘markle’ type) is also present and tuff and agglomerate are 

present at the base of the member in the small stream due 

south of the bridge over the River Carron [Ns 748 838]. 

Stratotype 

The type area is in the north-eastern Kilsyth Hills, north-east 

of Glasgow [Ns 7334 8238 to 7783 8401] (Forsyth et al., 

1996). A reference section is an unnamed tributary of the 

River Carron, north-east Kilsyth Hills [Ns 7479 8376 to 7486 

8365] (Craig, 1980). This shows the base of the member. 


The lower boundary of the Faughlin lava member is 

conformable or disconformable on the underlying Carron 

Bridge lava member, and is marked by a tuff overlying 

trachybasalt in the small stream due south of the bridge over 

the River Carron [Ns 748 838]. 

The Faughlin lava member is overlain by the Campsie 

lava member. The lithological change is to mostly plagioclase-microphyric 

basalt and trachybasalt (‘Jedburgh’ 

type). 

Thickness 

some 35 m 




The member is restricted to the eastern part of the Campsie 

Block (Forsyth et al., 1996), specifically to two small areas 

of the north-eastern Kilsyth Hills, north-east of Glasgow. 

The rocks crop out in a small area south and east of the 

Faughlin Reservoir, from Faughlin Burn [Ns 7336 8242] to 

the east of Carron Bridge [Ns 7484 8378], and in a separate 

area between langhill [Ns 7698 8426 ] and the west bank 

of the River Carron [Ns 7783 8401]. The source of this 

member is probably local. 

Age 


4.3.3.36 TaPPeTKnowe lava MeMBer 

Name 

previously named the Tappetknowe lavas (Forsyth et al., 

1996). 

Lithology 

The Tappetknowe lava member consists of several lavas 

with a total thickness of approximately 40 m. These 

include, near Tappetknowe [Ns 750 815], microporphyritic 

basaltic-trachyandesite (mugearite) and trachybasalt and 

rare plagioclase-macrophyric trachybasalt (‘markle’ type). 

The rocks are intensely faulted and jointed and deeply 

weathered, and there are no good sections, exposure being 

limited to small crags. 

Stratotype 

The type area is the central Kilsyth Hills, north of Glasgow 

[Ns 7176 8064 to 7622 8197] (Forsyth et al., 1996). 


The lower boundary is conformable or locally 

disconformable on the underlying laird’s loup lava 

member, which comprises plagioclase-macrophyric 

trachybasalt, and is taken as the incoming of 

microporphyritic lavas (basaltic-trachyandesite to 

trachybasalt). The Tappetknowe lava member is overlain 

to the north-east of the Tak-ma-doon Fault (Craig, 1980) 

by the denny muir lava member. The lithological 

change here is to massive, well-featured plagioclasemacrophyric 

basalt (of ‘markle’ type), trachybasalt and 

rare basaltic-trachyandesite (mugearite). 

To the south-west of the Tak-ma-doon Fault, the 

Tappetknowe lava member is overlain by the Kilsyth Hills 

lava member, and the lithological change is mainly to 

plagioclase-macrophyric basalts and trachybasalts (hawaiites 

of ‘markle’ type). 

Thickness 

some 40 m. 





These rocks crop out in the escarpment on the southern 

side of the Kilsyth Hills, north-east of Kilsyth, from south 

of Tomtain [Ns 7179 8062], eastward to the Tak-ma-doon 

Fault (Craig, 1980), thence to the north and south of doups 

[Ns 7494 8138] and as far east as Tappetknowe [Ns 7620 

8196]. Craig (1980) inferred that the source of the lavas was 

near to the present outcrop. 

Age 




38 

4.3.3.37 CaMPsie lava MeMBer 

Name 

previously referred to as four separate successions named 

the lower south Campsie lavas, lower North Campsie 

lavas, upper south Campsie lavas and upper North 

Campsie lavas (Craig, 1980; Forsyth et al., 1996; Hall et 

al., 1998). 

Lithology 

The Campsie lava member has been divided stratigraphically 

into lower and upper sequences and geographically into 

northern and southern sequences that reflect petrographically 

their source vent systems. Although the various sequences 

are distinctive in some areas, enabling their boundaries 

to be identified, elsewhere they interdigitate laterally and 

have no distinctive stratigraphical markers to separate 

them vertically. Hence it is not possible to draw continuous 

boundaries between them on a map and therefore they have 

all been assigned to a single formal member. The four 

sequences have been given informal names that have been 

widely used on maps and in literature (Craig, 1980; Forsyth 

et al., 1996; Hall et al., 1998). The informal sequences are 

the lower south Campsie lavas, the lower north Campsie 

lavas, the upper south Campsie lavas and the upper north 

Campsie lavas. 

The distinctive characteristic of the whole member is that 

it is composed almost entirely of plagioclase-microphyric 

basalt and trachybasalt (basaltic hawaiite and hawaiite) 

lavas (i.e. of ‘Jedburgh’ type). within this restricted range 

there is considerable petrographical variation and there are 

systematic variations between the south and north Campsie 

lavas. The south Campsie lavas contain significant amounts 

of clinopyroxene, whereas in the north Campsie lavas it 

is present only as small granules in the groundmass. The 

plagioclase microphenocrysts also differ, being labradorite 

to calcic andesine in the south but sodic andesine in the 

north. These variations reflect the whole-rock compositions, 

which are dominantly basalt to basaltic hawaiite 

in the south and hawaiite to mugearite in the north. The 

lower and upper Campsie lava sequences can be identified 

where they are separated locally by one of several other 

lava members of distinctly different petrography. These are 

the Craigentimpin lava member, the loup of Fintry lava 

member, the laird’s Hill lava member and the overton 

lava member. since it is not certain if those four members 

are contemporaneous, the boundaries between the lower 

and upper Campsie lavas, where drawn, do not necessarily 

involve lavas of exactly the same age everywhere. 

The lower south Campsie lavas are microporphyritic 

trachybasalts (basaltic hawaiite and hawaiite of ‘Jedburgh 

type’) with microphenocrysts of sodic labradorite and a 

generally quite high content of mafic minerals which have 

been extensively replaced, especially in the case of olivine 

and augite, by carbonate, as has some plagioclase. Basalt 

lavas also occur. in the western Campsie Fells, in the 

Forking Burn [Ns 653 790], there are ten proximal-facies 

lavas, totalling 80 m in thickness, showing toe structures 

and other features typical of pahoehoe lavas. These are separated 

by ‘slaggy’ agglomerates which make up about 25 

per cent of the total thickness of the section. The individual 

lavas are generally thin (3 to 8 m) and highly amygdaloidal. 

viriditic material is prominent in the groundmass. in the 

Garrel Burn [Ns 697 807], the lavas are thicker, more massive, 

less amygdaloidal, and more distal in character, and 

the total thickness is reduced to approximately 50 m. 

The lower north Campsie lavas consist mainly of olivinemicrophyric 

basalt and trachybasalt (basaltic hawaiite and 

hawaiite of ‘Jedburgh’ type). There is considerable modal

variation but clinopyroxene is generally lacking except as 

very small grains in the groundmass. plagioclase microphenocrysts 

tend to be in the sodic andesine range. The best 

section is in the western escarpment overlooking the Blane 

water valley at Black Craig [Ns 558 812] where nine lavas 

are present, although the lowest of these is interpreted as 

part of the lower south Campsie lavas (Craig, 1980; Hall 

et al., 1998). These form a near-vertical face with welldeveloped 

tuff and scoria, up to 2 m thick, at the top of 

each lava. The lowest three lavas are each approximately 

15 m thick, while the remainder are noteably thinner, averaging 

about 10 m each. Crude columnar jointing is evident 

in most of the lavas, except the second which locally has 

irregular subvertical platy jointing and comprises several 

‘flow units separated by rather impersistent slaggy layers’ 

(Craig, 1980). despite petrographical differences between 

the north and south Campsie lavas, it is not readily possible 

to distinguish between the two in all areas, and the two 

sequences are interpreted as interdigitating in many sections 

between the northern and southern Campsie Fells and 

Kilsyth Hills (Craig, 1980). 

The upper south Campsie lavas consist of microporphyritic 

trachybasalt (hawaiites of ‘Jedburgh’ type), transitional 

to basaltic-trachyandesite (mugearite) with a very 

low content of augite. These lavas are well exposed in the 

Goat Burn [Ns 637 793], above the southern escarpment 

in the eastern Campsie Fells, where a sequence of lavas, 

40 m thick, is developed. The sequence comprises four 

lavas, the lower three averaging 12 m in thickness, and the 

fourth 5 m. The third lava is compound, as may also be the 

lowest, which is poorly exposed. The uppermost lava, and 

one of the flow units of the compound third lava, die out 

eastwards, as does the sequence as a whole. 

The upper north Campsie lavas consists of plagioclasemicrophyric 

trachybasalt and some basalt (basalt to hawaiite 

of ‘Jedburgh’ type) with scoriaceous agglomerates and 

tuffs. Basaltic trachyandesite (mugearite) also occurs. The 

lavas are generally poorly exposed and there are few sections 

through them. in the muir Toll Burn [Ns 628 828] the 

total thickness is about 40 m, part of which is repeated by 

the south Campsie muir Fault. Farther east, on Cairnoch 

Hill [Ns 690 852], Haugh Hill [Ns 682 842] and little Bin 

[Ns 674 830], thick distal facies sequences occur, but are 

poorly exposed. in the Gonachan [Ns 602 838] and Clachie 

[Ns 612 840] burns, faulted sections, partly obscured 

by superficial deposits, occur. These are of proximalfacies 

lavas which are thin and carbonated, with considerable 

scoriaceous agglomerates and tuffs between the lavas. 

interdigitation with lavas derived from the south, which 

are more mafic and more basaltic than those of the upper 

north Campsie lavas, is characteristic. This appears likely 

to be the case in the central and western Campsie Fells, 

including Ballagan Burn Glen [north of Ns 5726 8043], 

Finglen [north of Ns 5956 8043] and Campsie Glen [north 

of Ns 6239 8080]. similar interdigitation is seen in the 

River Carron [between Ns 766 848 and Ns 771 846] in the 

easternmost Kilsyth Hills, where a sequence, dipping to the 

east, of five or six relatively thin trachybasalts, transitional 

to basaltic trachyandesite, is exposed. 

Stratotype 

The Campsie Fells and Kilsyth Hills, between strathblane 

[Ns 555 797] and the Carron valley, east to [Ns 785 833], 

north and north-east of Glasgow. 


in the northern Campsie Fells, the lower boundary of the 

Campsie lava member is taken as the first appearance 

39 

of basalt or trachybasalt lava on the underlying North 

Campsie pyroclastic member of the Clyde plateau volcanic 

Formation, and the contact appears to be conformable or 

disconformable. However, in the western and south-western 

Campsie Fells, the North Campsie pyroclastic member is 

absent and the Campsie lava member overlies the Clyde 

sandstone Formation of the inverclyde Group. Farther 

east in the southern Campsie Fells, at three localities 

between the Finglen Burn [Ns 599 800] and the Forking 

Burn [Ns 653 790], it rests directly, and unconformably, 

on argillaceous rock, dolostone and sandstone of the older 

Ballagan Formation of the inverclyde Group, suggesting 

that the lower boundary is an unconformity, both there 

and maybe also in the northern Campsie Fells. To the east 

of the east Bachille Fault [Ns 6915 7974] and west of 

the Chapmen’s Graves Fault [Ns 7063 8046], the lower 

boundary is taken as the first appearance of basalt or 

trachybasalt on the plagioclase-macrophyric trachybasalt 

(hawaiite) lavas of the laird’s loup lava member. 

in the central and western Campsie Fells, the Campsie 

lava member is overlain with apparent unconformity by 

the Fin Glen lava member. The lithological change is to 

trachyte, with basaltic trachyandesite (mugearite), trachybasalt 

(hawaiite) and basalt. in the eastern Campsie Fells 

and western Kilsyth Hills, the member is overlain variably 

disconformably to unconformably by the lower lecket 

lava member, and in some places the member was probably 

entirely removed by erosion prior to emplacement of 

the lower lecket lava member; for example south-east 

of Cort-ma law [Ns 6515 7995], south and east of Brown 

Hill [Ns 6645 7897] and around laird’s Hill [Ns 6957 

8018]. in the north-eastern Kilsyth Hills, the Campsie lava 

member is overlain, probably unconformably by the lavas 

of the Gargunnock Hills lava member, or in the south-east 

Kilsyth Hills, by the Kilsyth lava member. 

Thickness 



The Campsie lava member accounts for over 30 per cent 

of the outcrop of volcanic rocks in the structural Campsie 

Block, which comprises the Campsie Fells and Kilsyth 

Hills, north and east of Glasgow. it is present throughout 

the block with the exception of the southern escarpment 

between Garrel Hill [Ns 704 805] and Tappetknowe [Ns 

761 819]. 

The lower south Campsie lavas are generally restricted to 

the southern part of the block and are developed along most 

of the length of the southern Campsie Fells and southern 

Kilsyth Hills. They also crop out from the western Campsie 

Fells [Ns 5540 7977] eastwards, immediately to the north 

of the Campsie Fault, to the south sides of lairs [Ns 640 

791] and Brown Hill [Ns 665 785], to the south side of 

Garrel Hill [Ns 7068 8053]. They are also interdigitated 

with and undivided from, the lower north Campsie lavas, 

eastwards across the Kilsyth Hills, from the north-east of 

little Bin [Ns 6726 8339], to the south of the Carron valley 

Reservoir [Ns 700 825] to the lower western, southern and 

eastern flanks of dundaff Hill [Ns 7273 8486] to [Ns 7467 

8470], north of denny muir [Ns 7505 8254] and along 

the River Carron, north of Tarduff Hill [Ns 7486 8387] to 

[Ns 7580 8463], and to the west and east of Northshields 

[Ns 762 838] to [Ns 7783 8396]. The extent to which they 

extend farther northwards across the Campsie Fells and 

Kilsyth Hills is uncertain, but they are likely to be interdigitated 

with the lower north Campsie lavas across most 

of that area. 



The lower north Campsie lavas are generally restricted 

to the northern part of the Campsie Block and are developed 

along most of the length of the northern Campsie 

Fells and northern Kilsyth Hills. They crop out from the 

western Campsie Fells [Ns 5520 8180] eastwards, across 

Craigbarnet muir [Ns 575 835] to the endrick water [Ns 

6617 8619]. They are also interdigitated with and undivided 

from, the lower south Campsie lavas southwards across the 

Campsie Fells and Kilsyth Hills as detailed above. 

The upper south Campsie lavas are restricted to the 

southern part of the Campsie Block and are developed 

along most of the length of the southern Campsie Fells and 

southern Kilsyth Hills. They crop out in the escarpment 

north of the Campsie Fault, and extend westwards across 

the southern Campsie Fells to the Ballagan Burn [Ns 5726 

8043]. They also extend eastwards across the Kilsyth Hills 

to the River Carron [Ns 766 848] and [Ns 771 846], where 

they are interdigitated with the upper north Campsie lavas. 

The extent to which they extend northwards across the 

Campsie Fells and Kilsyth Hills is uncertain, but they might 

be interdigitated with the upper north Campsie lavas across 

most of the area. 

The upper north Campsie lavas are generally restricted 

to the northern part of the Campsie Block and are developed 

along most of the length of the northern Campsie 

Fells and northern Kilsyth Hills. These rocks crop out from 

the western Campsie Fells [Ns 562 820] eastwards, across 

Craigbarnet muir [Ns 575 830] to the Gonachan [Ns 602 

830] and Clachie [Ns 612 840] burns. They also extend 

eastwards across the Kilsyth Hills, where they are interdigitated 

with the upper south Campsie lavas as detailed 

above. 

Age 


4.3.3.38 CraigenTiMPin lava MeMBer 

Name 

previously named the Craigentimpin lavas (see Forsyth 

et al., 1996; also Hall et al., 1998; whyte and macdonald, 

1975). 

Lithology 

The Craigentimpin lava member consists of plagioclasemacrophyric 

basalt to trachybasalt (‘markle’ type) 

characterised by large phenocrysts of calcic labradorite. 

Two lava flows are present in the sloughmuclock area [Ns 

627 795]. elsewhere, it generally consits of only one lava. 

Stratotype 

The type area is the central Campsie Fells, north of Glasgow 

[Ns 6316 8244 to 6224 8399] (Forsyth et al., 1996). A 

reference section is the Alvain Burn [Ns 6180 8053 to 6179 

8060] (Craig, 1980). The member is also well exposed in 

Craigentimpin Quarry [Ns 616 802]. 


The base is conformable or disconformable on the underlying 

plagioclase-microphyric trachybasalt (hawaiite) lava of the 

lower north Campsie lavas (Campsie lava member) in 

the north of its outcrop, and by plagioclase-microphyric 

trachybasalt (hawaiite) lavas of the lower north Campsie 

and lower south Campsie lavas (Campsie lava member) in 

the south of its outcrop. 

The Craigentimpin lava member is overlain with 

apparent conformity by the upper north Campsie lavas 

(Campsie lava member) in the north of its outcrop and 

by the upper north Campsie and upper south Campsie 



40 

lavas (Campsie lava member) in the south of its outcrop. 

The lithological change is to mostly plagioclase-microphyric 

basalt to trachybasalt (hawaiite) lavas (‘Jedburgh’ 

type). 

Thickness 

Between 0 and about 30 m. The maximum thickness of the 

member is developed in the sloughmuclock area [Ns 627 

795], but it thins out completely to the west. 


The member is restricted to the Campsie Block (Forsyth 

et al., 1996) and specifically to the central and eastern 

Campsie Fells, north of Glasgow. These rocks crop out 

north of the Campsie Fault in two areas. The southernmost 

of the two areas extends along the lower part of the 

escarpment north of the Campsie Fault, to the south-west 

of lairs [Ns 6424 7994], from west of sloughneagh [Ns 

6532 7909] westwards to Craigentimpin Quarry [Ns 616 

802] and west to near Allanhead [Ns 6070 8036]. The 

northernmost of the two areas of outcrop is faulted and 

extends northwards, discontinuously, from the south side of 

Campsie muir [Ns 6316 8244], thence to its east and north, 

and to the eastern flanks of dunbrach [Ns 6224 8399]. 

According to whyte and macdonald (1974) the orientation 

of the feldspar phenocrysts suggest that the source of 

the lava was the waterhead Centre (‘waterhead Central 

volcanic-Complex’). 

Age 


4.3.3.39 louP oF FinTry lava MeMBer 

Name 

previously named the loup of Fintry lavas (Forsyth et al., 

1996). 

Lithology 

The loup of Fintry lava member consists of two lavas, 

separated by a thin bed of basaltic lapilli-tuff. The lower 

lava is a plagioclase-macrophyric trachybasalt (‘markle’ 

type). The upper lava is a composite flow of similar overall 

composition, with intermingling of aphyric and feldsparphyric 

components [Ns 656 858]. other exposures of the 

member include plagioclase-macrophyric lava at the northwest 

end of loch Carron [Ns 673 856] and near the spout 

of dalbowie [Ns 641 869]. 

Stratotype 

The type area is the north-eastern Campsie Fells, north-east 

of Glasgow [Ns 641 869 to 673 856] (Forsyth et al., 1996). 

A reference section is the loup of Fintry (waterfall), in the 

endrick water, north-eastern Campsie Fells, north-east of 

Glasgow from [Ns 6618 8617 to 6645 8612] (Craig, 1980). 

Here the full thickness of the member is evident. 


The lower (basal) plagioclase-macrophyric trachybasalt 

lava is conformable or disconformable on the underlying 

plagioclase-microphyric trachybasalt of the lower north 

Campsie lavas (Campsie lava member). 

The upper composite lava of the loup of Fintry lava 

member is overlain apparently conformably, or disconformably, 

by the upper north Campsie lavas (Campsie lava 

member). The lithological change is mostly to plagioclasemicrophyric 

basalt (‘Jedburgh’ type), trachybasalt and 

basaltic-trachyandesite (mugearite).

Thickness 

Nearly 30 m in the vicinity of the loup of Fintry [Ns 662 

862]. 



et al., 1996) and specifically to the north-eastern Campsie 

Fells, north-east of Glasgow. These rocks crop out in small 

isolated areas, in the vicinity of the loup of Fintry [Ns 662 

862], at the north-west end of loch Carron [Ns 673 856], 

and near the spout of dalbowie [Ns 641 869]. 

Age 


4.3.3.40 lairD’s Hill lava MeMBer 

Name 

previously named the laird’s Hill lavas (Forsyth et al., 

1996). 

Lithology 

The laird’s Hill lava member consists of only one or two 

lavas. in the stream sections to the north and west of Corrie 

Reservoir [Ns 674 791] it is represented by a single flow 

of plagioclase-macrophyric basalt (‘markle’ type), which 

is not shown on 1:50 000 scale sheet 31w (BGs, 1992). 

Farther north-east it consists of a similar flow, underlain by 

a basaltic-trachyandesite (mugearite) lava, both of which 

crop out near the summit of laird’s Hill [Ns 696 801] (the 

boundaries of the member here are difficult to delineate 

on both 1:50 000 and 1:10 000 scale maps). The two 

flows are also seen in various stream headwaters draining 

northwards to loch Carron, although relationships here are 

less clear due to poor exposure, and it is possible that there 

is interdigitation with other members. The source of the 

lavas is uncertain. 

Stratotype 

The type area is the central Kilsyth Hills, north-east of 


1996). A reference section is the Birken Burn, central 

Kilsyth Hills [Ns 6900 8046 to 6867 8051] (Craig, 1980). 

Here, good exposures of the lavas are found in the stream 

section. 


The basal plagioclase-macrophyric basalt, or locally 

basaltic-trachyandesite (mugearite), of the member 

is conformable or disconformable in the south on the 

underlying microporhyritic trachybasalt lava of the lower 

south Campsie lavas (Campsie lava member), and in the 

north, on the undivided microporphyritic trachybasalt lavas 

of the lower north Campsie and lower south Campsie lavas 

(Campsie lava member). 

The laird’s Hill lava member is overlain in the north 

by the undivided upper north Campsie and upper south 

Campsie lavas (Campsie lava member) and the lithological 

change is to microporphyritic trachybasalt. However, in the 

south, the Campsie lava member is absent due to erosion 

prior to deposition of the lower lecket Hill lava member, 

and the laird’s Hill lava member is overlain unconformably 

by basaltic-trachyandesite of the lower lecket Hill 

lava member. locally also, in the south, the laird’s Hill 

lava member is absent, presumably due to erosion prior to 

deposition of the lower lecket Hill lava member. 

Thickness 

some 20 m 

41 


The member is restricted to the Campsie Block (Forsyth et 

al., 1996) and specifically to the central part of the Kilsyth 

Hills, north-east of Glasgow. These rocks crop out in two 

main areas. one, on the northern side of the Campsie Fault 

extends eastwards from the east flank of Brown Hill [Ns 

6670 7913]. it is locally absent on the south-west flank 

of laird’s Hill from [Ns 6844 7964 to 6938 7996], but 

reappears on the south-east, east and north flanks of laird’s 

Hill [Ns 6957 8018]. The member is absent on plea muir 

[Ns 6934 8076]. The second area of outcrop extends from 

the north flank of Barrel Hill [Ns 7042 8158] westwards as 

far as the Burnhouse Burn on the south-east side of meikle 

Bin [Ns 6746 8194]. 

Age 


4.3.3.41 overTon lava MeMBer 

Name 

previously named the overton lavas (Forsyth et al., 1996). 

Lithology 

The overton lava member consists of at least one 

plagioclase-macrophyric basalt lava (‘markle’ type) 

overlying a basaltic-trachyandesite lava (mugearite). 

several lava flows, including trachybasalt, may be present. 

No source for the lavas has been identified. 

Stratotype 

The type area is the eastern Kilsyth Hills, north-east of 

Glasgow [Ns 7532 8120 to 7706 8434] (Forsyth et al., 1996). 

Best exposures are in the faulted River Carron section, to the 

north-west of Nicholswalls [Ns 764 843] and in the reference 

section in the overton Burn [Ns 7745 8353 to 7673 8344], 

east of overton, eastern Kilsyth Hills (Craig, 1980). 


The basal basaltic-trachyandesite (mugearite) lava of the 

member is conformable or disconformable in the north on 

the trachybasalt lavas of the undivided lower north Campsie 

and lower south Campsie lavas (Campsie lava member). 

elsewhere the base is not seen. 

The overton lava member in the east is overlain conformably 

or disconformably by the undivided upper north 

Campsie and upper south Campsie lavas (Campsie lava 

member), and in the north the member is overlain specifically 

by the upper north Campsie lavas (Campsie lava 

member). The transition is from plagioclase-macrophyric 

basalt lava to plagioclase-microphyric trachybasalt and 

some basalt lava (basalt to hawaiite of ‘Jedburgh’ type) with 

scoriaceous agglomerate and tuff. 

Thickness 

some 35 m 



al., 1996) and specifically to the eastern part of the Kilsyth 

Hills, north-east of Glasgow. These rocks crop out in two 

main areas. The first and principal area is in faulted ground 

to the south, east and north of darrach Hill [Ns 7537 

8276], from the east of doups [Ns 7533 8122], east to near 

meadowgreens [Ns 7765 8297], north to langhill [Ns 

7706 8432] and a stream east of Glenhead [Ns 759 852], 

with a small outlier west of the River Carron [Ns 7529 

8460]. The second area is a small outlier in the earl’s Burn 

[Ns 7175 8597 to 7129 8650]. 



Age 


4.3.3.42 langHill lava MeMBer 

Name 

previously named the langhill lavas (Forsyth et al., 1996). 

Lithology 

The langhill lava member consists of four flows of 

typically fine-grained, platy-jointed basaltic-trachyandesite 

(mugearite). The only exposures are in the River Carron 

[Ns 773 845] 500 m north-east of langhill. The lowest lava 

has a relatively coarse grain size and is about 15 m thick, 

with well-developed columnar jointing. The other lavas 

are very fine grained and intensely jointed. At least one of 

these has an autobrecciated base, consisting of buckled and 

disrupted tabular blocks of the lava. 

Stratotype 

The type area is the eastern part of the Kilsyth Hills [Ns 

7750 8442 to 7616 8539] (Forsyth et al., 1996). A reference 

section is the River Carron, eastern Kilsyth Hills, north-east 

of Glasgow [Ns 7726 8454 to 7749 8439] (Craig, 1980). 


The member overlies plagioclase-microphyric trachybasalt 

of the Campsie lava member, but the nature of the contact 

is unknown. 

The langhill lava member is overlain by the Gargunnock 

Hills lava member, but the nature of the contact is 

unknown. The lithological change is to mostly plagioclasemacrophyric 

basalt to hawaiite (‘markle’ type) with some 

plagioclase- and olivine-microphyric basalts (‘Jedburgh’ 

and ‘dalmeny’ types). 

Thickness 

some 35 m. 


The member is restricted to the eastern part of the Kilsyth 

Hills (Forsyth et al., 1996). The rocks mostly crop out on 

the northern side of the Carron Glen [Ns 7750 8442 to 

7616 8539] with the outcrop extending locally to the base 

of the valley [Ns 7739 8450] and on to the southern side 

[Ns 7709 6446]. 

Age 


4.3.3.43 lower leCKeT Hill lava MeMBer 

Name 

previously named the lower lecket Hiil lavas (Forsyth et 

al., 1996). 

Lithology 

The lower lecket Hill lava member consists of lavas 

of plagioclase-microphyric trachybasalt (hawaiite) (of 

‘Jedburgh’ type) to basaltic-trachyandesite (mugearite) 

and trachyandesite (benmoreite). Basaltic tuff-breccia and 

lapilli-tuff are present between the lavas. Along the southern 

escarpment of the Campsie Fells, the pyroclastic rocks are 

up to 4 m thick, and incorporate large scoria bombs. Craig 

(1980) interpreted these deposits as indicating derivation 

of at least some of the lower lecket Hill lava member 

from eruptive sources associated with the south Campsie 

linear vent system. in addition, in the vicinity of meikle 

Bin [Ns 6672 8217] and nearby to the south, the member is 

apparently interdigitated with tuff, interpreted as a tuff cone 



42 

deposit (Craig, 1980). in the Alnwick Burn [Ns 628 807 

to 636 803] there are at least seven successive lava flows. 

These are transitional between trachybasalt (hawaiite) and 

basaltic-trachyandesite (mugearite) and platy-jointing is 

common. only three lavas are present in the Goat Burn [Ns 

637 793] on the southern escarpment north of the Campsie 

Fault. The lowest of these is a trachyandesite (benmoreite) 

lava (Craig, 1980), 12 m thick, with well-developed platy 

jointing near its base and a crude columnar structure 

throughout the remainder of the unit. This is separated from 

a second lava, which is 5 m thick, by 2 m of ‘coarse and 

scoriaceous’ tuff (Craig, 1980). The third lava is of basaltictrachyandesite 

(mugearite), and is approximately 10 m 

thick. To the north of little Bin [Ns 673 831], the member 

is represented by a single lava of basaltic-trachyandesite 

(mugearite). 

Stratotype 

The type area is the easternmost Campsie Fells, and western 

Kilsyth Hills, north of Glasgow [Ns 6178 8000 to 6764 

8240] (Forsyth et al., 1996). A reference section is the 

Alnwick Burn, western Kilsyth Hills from [Ns 6284 8071 

to 6365 8057] where at least seven successive lavas have 

been identified (Craig, 1980). 


Across the northern and north-western parts of its outcrop, 

the base of the lower lecket Hill lava member appears 

to be conformable or disconformable on the underlying 

Campsie lava member. However, in the southern and 

south-eastern parts of its outcrop [Ns 6489 7904 to 7034 

8060] the base is unconformable on older members; on the 

southern flanks of Cort-ma law, the lower lecket Hill 

lava member rests unconformably on progressively older 

members from west to east, including the loup of Fintry 

lava member, and eventually [Ns 6548 7914] the Campsie 

lava member; and between the east flank of Brown Hill 

[Ns 6598 7890] and the south-west flank of Garrel Hill 

[Ns 7030 8065] the member rests unconformably either 

on the laird’s Hill lava member, or on the Campsie lava 

member. The unconformity may extend to the western 

limit of outcrop [Ns 6178 8000] where there appears to be 

thinning of the underlying Campsie lava member. 

The lower lecket Hill lava member is generally 

overlain with apparent conformity or disconformity by the 

Boyd’s Burn lava member, whose geographical extent is 

similar to that of the lower lecket Hill lava member. The 

lithological change is mostly to plagioclase-macrophyric 

hawaiite lavas (‘markle’ type). However, in the meikle Bin 

area [Ns 667 822], lavas of the lower lecket Hill lava 

member pass directly upwards into the remnant of the 

tephra cone associated with the meikle Bin Trachytic vent 

(waterhead Centre). 

Thickness 

some 50 m at Alnwick Burn [Ns 628 807 to 636 803]; 29 m 

thick at Goat Burn [Ns 637 793] (Craig, 1980). 



et al., 1996) and has a limited geographical extent in the 

easternmost Campsie Fells and western Kilsyth Hills, north 

of Glasgow. These rocks mostly crop out in the escarpment 

north of the Campsie Fault, to the south-west of lairs [Ns 

6424 7994], and on the southern flanks of Cort-ma law 

[Ns 6515 7995]. They also crop out: on the upper flanks of 

Brown Hill [Ns 6645 7897], but not on the summit; on the 

upper flanks of laird’s Hill [Ns 6957 8018]; on plea muir

[Ns 691 808] east to the south flank of Garrel Hill [Ns 7044 

8104]; on the lower eastern, northern and western flanks of 

lecket Hill [Ns 6445 8121], including the Alnwick Burn 

valley [Ns 632 805] ; and on the lower slopes of meikle 

Bin [Ns 6672 8217]. 

Age 


4.3.3.44 BoyD’s Burn lava MeMBer 

Name 

previously named the Boyd’s Burn lavas (see Forsyth et 

al., 1996). 

Lithology 

The Boyd’s Burn lava member consists of plagioclasemacrophyric 

trachybasalt (hawaiite of ‘markle’ type) lavas. 

These show a marked variation in the concentration and 

size of the plagioclase phenocrysts both between and within 

flows. There are basaltic lapilli-tuffs between the lavas. in 

the Boyd’s Burn area [Ns 650 814], at least four lavas with 

proximal-facies characteristics occur and tuffs between the 

lavas are well developed. These lavas have a rather ‘slaggy’ 

and decomposed nature, and are thought to be derived 

from the waterhead Centre (‘waterhead Central volcanic 

Complex’) (see Craig, 1980). in the Goat Burn section [Ns 

637 793] a lava, 12 m thick, of plagioclase-macrophyric 

trachybasalt (hawaiite) is overlain by a compound flow 

with three ‘flow units’ (Craig, 1980) totalling almost 15 m 

in thickness. These lavas are texturally quite variable with 

rather sparsely distributed plagioclase phenocrysts in a 

pale groundmass. Farther to the east, a similar sequence is 

exposed in the Burniebraes Burn [Ns 662 794], although 

faulting and the coincidence of stratigraphical dip and 

topographical slope partly obscure the relationships. Here, 

however, a third lava with numerous large plagioclase 

phenocrysts overlies the two lavas seen in the Goat’s Burn 

section. 

Stratotype 

The type area is the eastern Campsie Fells, and westernmost 


8294] (Forsyth et al., 1996). A reference section is Boyd’s 

Burn, westernmost Kilsyth Hills [Ns 6527 8167 to 6487 

8126] (Craig, 1980). The member is also quite well exposed 

in cliff sections along the southern escarpment of the 

Campsie Fells, north of the Campsie Fault. 


The basal plagioclase-macrophyric hawaiite lava of the 

member is conformable or disconformable on the underlying 

basaltic-trachyandesite (mugearite) of the lower lecket 

Hill lava member. 

The Boyd’s Burn lava member is overlain conformably 

or disconformably by the upper lecket Hill lava member. 

The lithological change is to mostly more-felsic lavas, 

including two basal basaltic-trachyandesite (mugearite) 

lavas, trachybasalt, and trachyte, but also including plagioclase-microphyric 

basalt to trachybasalt (‘Jedburgh’ type). 

Thickness 

Between 37 and 50 m. The maxium thickness is developed 

in the Boyd’s Burn area [Ns 650 814]. 



et al., 1996) and has a limited geographical extent, 

43 

(reflecting the proximal character of the lavas) in the 

eastern Campsie Fells and westernmost Kilsyth Hills, 

north of Glasgow. These rocks mostly crop out in the 

escarpment north of the Campsie Fault, to the south-west 

of lairs [Ns 6424 7994], and on the southern flanks of 

Cort-ma law [Ns 6515 7995]. They also crop out: in 

a small outlier on Brown Hill [Ns 6645 7897]; to the 

south, east and north-east of Box law [Ns 6669 7973]; 

on the eastern, northern and western flanks of lecket 

Hill [Ns 6445 8121]; and in an outlier at little Bin [Ns 

6725 8285]. 

Age 


4.3.3.45 Fin glen lava MeMBer 

Name 

previously named the Fin Glen lavas (Forsyth et al., 1996; 

see also Craig, 1980; Hall et al., 1998). 

Lithology 

The Fin Glen lava member consists of trachyte and 

feldspar-microphyric varying to aphyric basaltictrachyandesite 

(mugearite) transitional to trachybasalt 

(hawaiite) to basalt (of ‘Jedburgh’ type). Basaltic 

pyroclastic rock is present between many of the lavas. 

in all but the south-west and south-east, the base of the 

member is a phonolitic trachyte lava, characterised by 

well-developed planar jointing. This may be derived 

from a phonolite intrusion in the ‘North Campsie linear 

vent system’ near Fintry [Ns 614 863], to the north 

(Craig, 1980), which is one of very few phonolitic 

lavas in the Carboniferous and permian successions 

of northern Britain. in the southern part of its outcrop, 

another trachyte lava occurs near the top of the member. 

The wide variation in characteristics of the lavas and 

high degree of their interdigitation suggests individual 

lavas may have been erupted from different sources, 

some local and others more distant (Craig, 1980). 

Between the Fin Glen and the tributary of the Almeel 

Burn, and near the summit of owsen Hill [Ns 571 823] 

and dumbreck [Ns 574 815], to the east of Fin Glen, 

the lavas are highly scoriaceous and rubbly breccias 

are present. These resemble autobrecciated aa lavas, 

and have been interpreted (Craig, 1980) as distal lavas. 

in the Aldessan Burn [Ns 608 807] at least five lavas 

are exposed. The basal trachyte is pink weathering and 

intensely platy-jointed, with extensive brecciation, some 

of which appears to be autobrecciation. The remainder of 

the lavas are thinner and often sparsely feldspar-phyric. 

significant thicknesses of basaltic scoriaceous tuffbreccia 

and lapilli-tuff occur between most of the lavas. 

Stratotype 

The type area is western and central Campsie Fells, north 

of Glasgow [Ns 5760 8058 to 6210 8405] (Forsyth et 

al., 1996). A reference section is Aldessan Burn, central 

Campsie Fells, north of Glasgow [Ns 6079 8066 to 6072 

8091] (Craig, 1980). 


The basal phonolitic trachyte lava is conformable or 

disconformable on plagioclase-microphyric trachybasalt 

(hawaiite) lava of the Campsie lava member. 

The Fin Glen lava member is overlain by the 

Holehead lava member. The lithological change is 

mostly to plagioclase-macrophyric olivine basalts and 

trachybasalts (basalts to hawaiites of ‘markle’ type), 



characterised by the presence of variable amounts of 

generally small plagioclase macrophenocrysts. 

Thickness 

Between 60 and 110 m. The thickest development is on the 

east side of Fin Glen Burn [Ns 581 816], but this area is 

faulted, and exposure is only sporadic. 



et al., 1996) and specifically to the western and central 

Campsie Fells, north of Glasgow. These rocks crop out in 

high ground north of the Campsie Fault, on the summits 

of: dumbreck [Ns 5736 8149], and including the ridge to 

its south [Ns 5835 8066]; owsen Hill [Ns 5714 8233]; 

Hog Hill [Ns 592 822], including the area to the north and 

the lower flanks to the south-west and south; and Hart Hill 

[Ns 6043 8266], including the flanks to the north and east. 

The rocks also crop out around Fassis [Ns 604 806] and 

extending both to its north-west [Ns 5970 8165] and east 

[Ns 6226 8101]; on the lower flanks to the south-east, east 

and north-east of Holehead [Ns 6176 8262]; and in crags 

to the north-east, and on the eastern, northern and western 

flanks, of dunbrach [Ns 6147 8375]. 

Age 


4.3.3.46 uPPer leCKeT Hill lava MeMBer 

Name 

previously named the upper lecket Hiil lavas (Forsyth et 

al., 1996). 

Lithology 

The upper lecket Hill lava member consists generally of 

relatively felsic lavas, including trachybasalt (hawaiite), 

basaltic trachyandesite (mugearite), trachyte and rare 

plagioclase-microphyric basalt transitional to trachybasalt 

(of ‘Jedburgh’ type). The member is generally poorly 

exposed, but a reasonable section is present in the Back 

Burn [Ns 640 803], where at least seven platy-jointed and 

rather ‘slaggy’ lavas are present. in Goat Burn [Ns 637 

794] two lavas (or ‘flow units’ of Craig, 1980) of basaltictrachyandesite 

(mugearite) are overlain by a lava, 6 m thick, 

of trachybasalt (hawaiite), above which is a compound 

15 m-thick lava of very fine-grained ‘slaggy’ trachybasalt 

(hawaiite) or basaltic-trachyandesite (mugearite) with 

scattered small feldspar phenocrysts, and a pale-weathered, 

platy-jointed basaltic-trachyandesite (mugearite), 5 m thick. 

The top of the section is obscured by peat. North-east of 

the summit of lecket Hill [Ns 6445 8121], lapilli-tuffs and 

agglomerates locally predominate over lavas, which include 

trachyte. 

Stratotype 

The type area is the eastern Campsie Fells, and westernmost 


8094] (Forsyth et al., 1996). A reference section through the 

member is seen at Back Burn [Ns 6371 8021 to 6489 8033] 

(Craig, 1980), and an incomplete section is present along 

the southern escarpment of the Campsie Fells, north of the 

Campsie Fault at Goat Burn [Ns 637 794]. 


The basal basaltic-trachyandesite (mugearite) lava of 

the member is conformable or disconformable on the 

underlying plagioclase-macrophyric trachybasalt (hawaiite) 

lava of the Boyd’s Burn lava member. 



44 

The upper lecket Hill lava member is overlain apparently 

conformably or disconformably by the Kilsyth Hills 

lava member, which has a similar geographical distribution. 

The lithological change is to plagioclase-macrophyric 

transitional to plagioclase-microphyric basalt and trachybasalt 

(hawaiite) lavas (of ‘markle’ type transitional to 

‘Jedburgh’ type). 

Thickness 

some 65 m 



al., 1996) and has a limited geographical extent, (reflecting 

the proximal character of the lava flows) in the eastern 

Campsie Fells and westernmost Kilsyth Hills, north of 

Glasgow. These rocks mostly crop out immediately above 

the escarpment north of the Campsie Fault, to the south-west 

of lairs [Ns 6424 7994], and on the southern, eastern and 

northern flanks of Cort-ma law [Ns 6515 7995], and on the 

upper flanks, but not the summit area, of lecket Hill [Ns 

6445 8121]. They also crop out in a very small outlier on the 

summit of little Bin [Ns 6725 8285]. Craig (1980) inferred 

that the source of the member was the nearby waterhead 

Centre (‘waterhead Central volcanic Complex’). 

Age 


4.3.3.47 HoleHeaD lava MeMBer 

Name 

previously named the Holehead lavas (Forsyth et al., 1996; 

see also Craig, 1980; Hall et al., 1998). 

Lithology 

The Holehead lava member consists mainly of plagioclasemacrophyric 

olivine basalts and trachybasalts (basalts to 

hawaiites of ‘markle’ type), characterised by the presence of 

variable amounts of relatively small plagioclase phenocrysts. 

in addition, one lava of transitional trachybasalt to mugearite 

composition is exposed in the middle of a lava sequence in 

the Alvain Burn [Ns 614 815]. in the Aldessan Burn [Ns 

607 809 to Ns 605 816], there is a sequence of seven lavas. 

The flows tend to be relatively thin with ‘slaggy’ tops and 

locally rubbly bases. 

Stratotype 

The type area is central Campsie Fells, north of Glasgow 

[Ns 5894 8166 to 6200 8341] (Forsyth et al., 1996). A 

reference section is Aldessan Burn, central Campsie Fells, 

north of Glasgow [Ns 6072 8092 to 6039 8224] where 

seven lavas are seen (Craig, 1980). 


The basal plagioclase-macrophyric basalt, and/or 

trachybasalt, is conformable or disconformable on basaltictrachyandesite 

(mugearite) of the Fin Glen lava member. 

The Holehead lava member occupies summit areas 

across its outcrop and the top of the member has been 

eroded. 

Thickness 

more than 100 m, top eroded. 



et al., 1996) and has a limited geographical extent in the 

Central Campsie Fells, north of Glasgow. These rocks

mostly crop out: in an outlier on the upper, southern flanks 

of Hog Hill [Ns 592 822]; around inner Black Hill [Ns 

6101 8164]; and around the summit of Holehead [Ns 6176 

8262]. The lavas were thought by Craig (1980) to have been 

derived from the waterhead Centre (‘waterhead Central 

volcanic Complex’). 

Age 


4.3.3.48 KilsyTH Hills lava MeMBer 

Name 

previously named the Kilsyth Hills lavas (Forsyth et al., 

1996). 

Lithology 

The Kilsyth Hills lava member consists predominantly 

of plagioclase-macrophyric basalts and trachybasalts 

(hawaiites of ‘markle’ type). The lower of these lavas 

tend to have sparse and small plagioclase phenocrysts and 

are transitional to plagioclase-microphyric basalts and 

trachybasalts (hawaiites of ‘Jedburgh’ type). some higher 

lavas in the sequence are olivine-augite-macrophyric 

basalts (of ‘dunsapie’ type) although these are always 

subordinate to the plagioclase-phyric lavas. Also, there 

is a local intercalation of variably olivine- and olivineaugite-microphyric 

basalt lava (‘Jedburgh’ to ‘dalmeny’ 

type). 

Stratotype 

The type area is in the central Kilsyth Hills, north-east of 


1996). A reference section is the crags on the southern 

flanks of Tomtain Hill, central Kilsyth Hills [Ns 7231 8072 

to 7212 8140] (Craig, 1980). 


over most of its outcrop, the base is conformable or 

disconformable on basaltic-trachyandesite (mugearite) and/ 

or trachybasalt (hawaiite) of the upper lecket Hill lava 

member. However, towards the south-east, the member 

rests unconformably on progressively older members 

until, in the Garrel Hill area [Ns 698 810], it rests on 

basaltic-trachyandesite (mugearite) of the lower lecket 

Hill lava member. south of Garrel Hill [Ns 750 806] it is 

directly underlain by plagioclase-microphyric trachybasalt 

(hawaiite) lava of the Campsie lava member, and to the 

south of Tomtain [Ns 7179 8062] and as far east as the Takma-doon 

Fault [Ns 7396 8106] it is underlain by basaltictrachyandesite 

(mugearite) and/or trachybasalt (hawaiite) of 

the Tappetknowe lava member. 

The Kilsyth Hills lava member occupies summit areas 


eroded. 

Thickness 

The member is most thickly developed on Tomtain [Ns 721 

814], where its apparent thickness is 160 m. Top eroded. 



et al., 1996) and specifically to the central Kilsyth Hills, 

north-east of Glasgow. The rocks crop out in the highest 

ground above the escarpment north of the Campsie Fault, 

to the west and around the summits of lairs [Ns 6424 

7994], Cort-ma law [Ns 6515 7995] and lecket Hill [Ns 

6445 8121]. The member also crops out in a separate area 

extending from the west of Garrel Hill [Ns 7044 8105], 

45 

around its north and south flanks, and around those of 

Tomtain Hill [Ns 721 814], as far east as the Tak-ma-doon 

Fault [Ns 7396 8109 to 7300 8196]. it is exposed in crags 

on high ground from Crighton’s Cairn [Ns 625 799] and 

lecket Hill [Ns 645 812] eastwards to the Tak-ma-doon 

Fault [Ns 7396 8109 to 7300 8196] (Craig, 1980). The 

member is equivalent laterally to the denny muir lava 

member which is recognised to the east of the Tak-ma-doon 

Fault. The lavas were thought by Craig (1980) to have been 



Age 


4.3.3.49 Denny Muir lava MeMBer 

Name 

previously named the denny muir lavas (see Forsyth et 

al., 1996). 

Lithology 

The denny muir lava member consists mostly of massive, 

well-featured plagioclase-macrophyric basalt or trachybasalt 

(‘markle’ type), trachybasalt lavas and rare basaltic 

trachyandesite (mugearite) lavas. The basal lava east of 

darrach Hill [Ns 754 827] is composite, with intermingled 

components of plagioclase-macrophyric and plagioclasemicrophyric 

basalt or trachybasalt (‘markle’ and ‘Jedburgh’ 

types respectively). The remainder of the lavas are massive 

and well featured, for example west of Birns [Ns 761 823]. 

An intensely jointed and ‘slaggy’ basaltic-trachyandesite 

(mugearite) lava occurs in faulted ground in the headwaters 

of the Garvald Burn [Ns 758 825]. 

Stratotype 

The type area is the eastern Kilsyth Hills, north-east of 


1996). A reference section is the crags west of Birns, 

eastern Kilsyth Hills [Ns 7555 8228 to 7559 8228] (Craig, 

1980). 


To the north and east, the base, locally a composite 

lava, is conformable or disconformable on underlying 

plagioclase-microphyric trachybasalt lavas of the Campsie 

lava member, but towards the south-west, where these 

lavas are absent, the member rests directly on plagioclasemicrophyric 

basaltic-trachyandesite and/or trachybasalt, 

of the Tappetknowe lava member, suggesting that the 

boundary is an unconformity. 

The denny muir lava member occupies summit areas 


eroded. 

Thickness 

up to 85 m 



et al., 1996) and specifically to the eastern Kilsyth Fells, 

north-east of Glasgow. These rocks crop out in high ground 

north of the Campsie Fault, and to the east of the Tak-madoon 

Fault [Ns 7396 8109 to 7300 8196], across denny 

muir [Ns 750 830], and around darrach Hill [Ns 7538 

8275]. in addition, there is a small outlier around the top 

of Tarduff Hill [Ns 756 836]. The lavas are essentially 

continuous with those of the Kilsyth Hills lava member 

which lie to the west of the Tak-ma-doon Fault (Craig, 



1980). The lavas were thought by Craig (1980) to have been 



Age 


4.3.3.50 KnoweHeaD lava MeMBer 

Name 

previously named the Knowehead lavas (Forsyth et al., 

1996; see also Craig, 1980; Hall et al., 1998). 

Lithology 

The Knowehead lava member consists of a broad 

range of petrographical types, including plagioclasemacrophyric 

trachybasalt lavas (hawaiites of ‘markle’ 

type), olivine- augite-plagioclase-macrophyric basalt 

(‘dunsapie’ type), plagioclase-microphyric trachybasalt 

(hawaiite), basaltic-trachyandesite (mugearite), and a 

rhyolite lava of restricted extent of exposure. The 

rhyolite has fine platy joints ‘with streaky flow-banding 

picked out in pale and red weathering colours’ (Craig, 

1980). The outcrop is extensively faulted and it has not 

been possible to erect an internal stratigraphy for the 

member. The numerous intercalations of coarse tuff and 

the ‘slaggy’ tongue-like character of some of the lavas, 

led Craig (1980) to suggest that at least some of the lavas 

are close to their eruptive source, although no vents have 

been identified. 

Stratotype 

The type area is the south side of the central Campsie Fells, 

north of Glasgow [Ns5660 7965 to 6238 7940] (Forsyth 

et al., 1996). The member is best exposed in the Fin Glen 

Burn [Ns 604 794]. Craig (1980) made no attempt to erect a 

lava flow stratgraphy within the member due to the heavily 

faulted nature of the exposed section. 


The Knowehead lava member is fault bounded and the 

lower and upper boundaries are not seen. 

Thickness 

Greater than 50 m. 




side of the Campsie Fells, north of Glasgow. These rocks 

crop out on the south side of the Campsie Fault, in lower 

ground below the escarpment, bounded by the Campsie 

Fault to the north, and another west-north-west-trending 

fault to the south. The crop extends from east of Clachan of 

Campsie [Ns 6238 7940], to the north-east of lennoxtown, 

westwards to the Fin Glen Burn [Ns 604 794] and beyond 

to strathblane [Ns 5660 7965]. The outcrop was thought by 

Craig to extend farther west (Craig, 1980), but correlation 

in that area with the similar Cochno lava member of the 

Kilpatrick Hills succession (Hall et al., 1998), and farther 

to the south, is uncertain. 

Age 


4.3.3.51 CraigDouFFie lava MeMBer 

Name 

previously named the Craigdouffie lavas (see Forsyth et 

al., 1996). 



46 

Lithology 

The Craigdouffie lava member consists of a sequence 

of at least four lavas, comprising alternating plagioclasemacrophyric 

basalt or trachybasalt (basalt to hawaiite 

of ‘markle’ type) and aphyric basaltic-trachyandesite 

(mugearite), all with proximal-facies characteristics (Craig, 

1980). 

Stratotype 

The type area is the south-eastern Kilsyth Hills, north-east 


1996). The only reference section is Craigdouffie Burn, 

south-eastern Kilsyth Hills [Ns 7484 8074 to 7438 8072] 

where at least four lavas, at least 15 m thick in total, are 

seen at the top of the member (Craig, 1980; Forsyth et al., 

1996). 


The base of the Craigdouffie lava member is faulted and 

unseen. it is overlain by poorly exposed volcaniclastic 

sedimentary rocks of the Kirkwood Formation of the 

strathclyde Group. The lithological change is from basalt or 

trachybasalt to tuffaceous mudstone and tuff, but the nature 

of the contact is not known. 

Thickness 

more than 15 m, base not seen. 


The member is restricted to a small area adjacent to the 

south side of the Campsie Fault and adjacent to the northeast 

side of the Tak-ma-doon Fault (Craig, 1980), in the 

south-eastern Kilsyth Hills, north-east of Glasgow. These 

rocks crop out east-north-east of drumnessie, mainly 

in the Craigdouffie Burn [Ns 7448 8072 to 7484 8074] 

and on its northern side to [Ns 7479 8078]. The source 

is probably an undetected vent in the immediate vicinity 

(Craig, 1980). 

Age 


4.3.3.52 Corrie lava MeMBer 

Name 

previously named the Corrie lavas (see Forsyth et al., 

1996). 

Lithology 

The Corrie lava member consists of plagioclasemacrophyric 

basalt and trachybasalt lavas (‘markle’ type), 

aphyric basaltic-trachyandesite (mugearite) lava, and lapillituff 

and tuff-breccia beds. 

Stratotype 

The type area is in the south-western Kilsyth Hills, north 


1996). A reference section is an unnamed burn crossing the 

escarpment north of Corrie, south-western Kilsyth Hills 

[Ns 6904 7939 to 6892 7966] (Craig, 1980), but neither the 

lower nor upper boundary is seen. 


The Corrie lava member is fault-bounded and neither the 

lower or upper boundary is seen. 

Thickness 

more than 30 m (Forsyth et al., 1996, table 3). Neither top 

nor base is seen.




side of the south-western Kilsyth Hills, north of Glasgow. 

The outcrop is bounded to the south by the Campsie Fault, 

to the north by the Bachille Fault and to the north-east by 

the east Bachille Fault (Craig, 1980). These rocks crop out 

in faulted ground below the escarpment on the southern 

side of the Kilsyth Hills, north-west of Kilsyth, from the 

west of Corrie plantation [Ns 6820 7909], eastwards to the 

north-east of Corrie [Ns 6952 7957]. derivation is thought 

to have been from local vents (Craig, 1980). 

Age 


4.3.3.53 garvalD lava MeMBer 

Name 

previously named the Garvald lavas (Forsyth et al., 1996). 

Lithology 

The Garvald lava member is well exposed in sections 

in the River Carron [Ns 781 838] and the overton 

Burn [Ns 7789 8350], where the member consists, in 

downward succession, of plagioclase-microphyric basalts 

or trachybasalts (basalts or hawaiites of ‘Jedburgh’ type), 

an olivine-augite-plagioclase-macrophyric trachybasalt 

(hawaiite of ‘dunsapie’ type), a prominently exposed 

microporphyritic basaltic-trachyandesite (mugearite), two 

plagioclase-macrophyric trachybasalts (hawaiite of ‘markle’ 

type), and a plagioclase-microphyric trachybasalt (hawaiite 

of ‘Jedburgh’ type) with pillow structures, indicating 

subaqueous emplacement (Craig, 1980). 

Stratotype 

The type area is the easternmost Kilsyth Hills, north-east 


1996). A reference section is the overton Burn, eastern 

Kilsyth Hills [Ns 7854 8324 to 7750 8355] though, as 

elsewhere, the base is not seen (Craig, 1980). 


The base is not seen, due to faulting. The Garvald lava 

member is overlain with angular unconformity by the 

Kirkwood Formation of the strathclyde Group. in the 

Garvald Burn section [Ns 781 838] the lithological change 

is from plagioclase-microphyric basalt or trachybasalt to 

volcaniclastic conglomerates and sandstones, which rest 

on progressively older lavas of the Garvald lava member 

towards the south. 

Thickness 




al., 1996) and specifically to the easternmost Kilsyth Fells, 

north-east of Glasgow. These rocks crop out in faulted 

ground north of the Campsie Fault, from west of myot Hill 

[Ns 7720 8210], north-eastwards to Garvald [Ns 7849 

8335], north-north-west along the Carron Glen and then 

towards Buckleside [Ns 7744 8530]. The source is thought 

to be local, either a neck exposed in the River Carron, northeast 

of Northshields [Ns 779 840] or some other obscured 

source (Craig, 1980). 

Age 


47 

FINTRY – TOUCH BLOCK (Fintry Hills, Gargunnock 

Hills, Touch Hills) 

Note that there are local variations in the general 

stratigraphy as presented. This is related to interdigitation 

and unconformities, and the restricted distribution and 

multiple sources of some of the members. 

4.3.3.54 slaCKDown lava MeMBer 

Name 

previously known as the Basal Group (Francis et al., 1970). 

Lithology 

The slackdown lava member consists of a varied 

assemblage of dominant trachybasalt lavas, with 

plagioclase-macrophyric basalt lavas (‘markle’ type) and 

plagioclase-microphyric basalt lavas (‘Jedburgh’ type). in 

crags north of scout Head (see Stratotype below) a basaltictrachyandesite 

(mugearite), or albitised trachybasalt lava, 

which is variably massive to platy-jointed, is overlain 

in succession by a thin and impersistent plagioclasemacrophyric 

basalt lava, a plagioclase-microphyric basalt 

lava, and a generally massive trachybasalt, transitional to 

plagioclase-microphyric basalt lava. 

Stratotype 

The type area is in the northern Touch Hills, and the 

northern and north-eastern Gargunnock Hills, north-east 

of Glasgow [Ns 6576 9125 to 7410 9372] (Francis et 

al., 1970). A reference section is provided by the crags 

north of scout Head, northern Touch Hills [Ns 7311 

9352 to 7315 9340]. largely obscured by drift, it is 31 m 

thick. The lavas form a series of cliffs at the foot of the 

escarpment and the basal mugearite forms a particularly 

prominent and laterally extensive crag (Francis et al., 

1970). 


The basal basaltic-trachyandesite (mugearite) of the member 

unconformably overlies sedimentary rocks, including 

sandstone, siltstone and mudstone of the Clyde sandstone 

Formation, of the inverclyde Group. 

The slackdown lava member is overlain, conformably 

or disconformably, by the Baston Burn lava member. The 

lithological change is from trachybasalt to plagioclase-macrophyric 

basalt (‘markle’ type), except in the north-western 

Gargunnock Hills, where the uppermost slackdown lava 

member is represented by plagioclase-microphyric basalt 

(‘Jedburgh’ type). 

Thickness 



The member is restricted to the Fintry–Touch Block 

(Francis et al., 1970) and specifically to the northern Touch 

Hills and the north-eastern Gargunnock Hills. These rocks 

crop out east-north-eastwards, from the north of lees Hill 

[Ns 6576 9125] to the north-north-east, to the Baston Burn 

[Ns 7410 9372]. 

Age 


4.3.3.55 sKiDDaw lava MeMBer 

Name 

previously named the skiddaw Group (Francis et al., 

1970). 



Lithology 

The skiddaw lava member consists predominantly 

of plagioclase-macrophyric basalt (‘markle’ type) and 

composite lavas with some plagioclase-microphyric basalt 

(‘Jedburgh’ type). in the east of the outcrop [Ns 6572 9122] 

the member comprises coarse olivine basalt at the base, above 

which the sequence comprises: a plagioclase-macrophyric 

basalt lava, a composite lava composed of massive, rounded 

bodies mostly of plagioclase-macrophyric basalt, but also 

including near the centre of the lava some transitional 

plagioclase-microphyric to olivine-microphyric basalts, 

in a matrix of ‘slaggy’, highly vesicular microporphyritic 

basalt; and a massive, transitional plagioclase-microphyric 

to plagioclase-macrophyric basalt with traces of columnar 

jointing. 

Stratotype 

The type area is in the northern and western Fintry Hills, 

and the north-western Gargunnock Hills, north-east of 

Glasgow [Ns 6304 8712 to 6577 9122] (Francis et al., 

1970). A reference section is at slackgun, north-western 

Gargunnock Hills [Ns 6572 9122] where a section 34 m 

thick (apparently the full thickness at this locality) was 

given by Francis et al. (1970). 


The basal basalt lava of the member unconformably 

overlies sedimentary rocks, including sandstone, siltstone 

and mudstone of the Clyde sandstone Formation, of the 

inverclyde Group. 

The skiddaw lava member is overlain unconformably 

by the slackgun volcaniclastic member. The lithological 

change is from transitional plagioclase-macrophyric to plagioclase-microphyric 

basalt lava or composite basalt lava to 

a dull red bole reflecting prolonged weathering of the lavas. 

Thickness 



The member is restricted to the northern Fintry–Touch Block 

(Francis et al., 1970) and specifically to the northern and 

western Fintry Hills and to the north-western Gargunnock 

Hills, north-east of Glasgow. These rocks crop out from 

below double Craigs [Ns 6304 8712] north-north-west 

towards skiddaw [Ns 622 891] and then north-east, to the 

north-west side of lees Hill [Ns 6577 9122]. 

Age 


4.3.3.56 BasTon Burn lava MeMBer 

Name 

previously named the Baston Burn Group (see Francis et 

al., 1970). 

Lithology 

The Baston Burn lava member consists predominantly of 

plagioclase-macrophyric basalt lavas (‘markle’ type) with 

a few plagioclase-microphyric lavas, or microporphyritic 

components of composite lavas (‘Jedburgh’ type). The 

member has eroded to form a prominent and wide step in 

the cliffs above the slackdown lava member in the northern 

Touch and Gargunnock hills. in the extreme east [Ns 7315 

9339 to 7318 9331], the member comprises three plagioclasemacrophyric 

basalt lavas, but farther west [Ns 7232 9320 

to 7234 9297] comprises four such lavas, the lower and 

upper two being separated by a thin lava composed of 



48 

microporphyritic basalt (‘Jedburgh’ type) (although this may 

be a component of a composite lava). in the Gargunnock 

Burn [Ns 7073 9292 to 7060 9267], the member lies in a 

shallow synclinal structure and comprises more than ten 

lavas. All are of plagioclase-macrophyric basalt except 

for the highest and lowest, which are transitional between 

macroporphyritic and microporphyritic basalt. The lowest 

lava is composite elsewhere [Ns 7154 9305]. 

Stratotype 

The type area is in the northern Touch Hills and Gargunnock 

Hills, north-east of Glasgow [Ns 6580 9120 to 7351 

9352] (Francis et al., 1970). A reference section is in 

the Gargunnock Burn, central northern Gargunnock Hills 

[Ns 7073 9292 to 7060 9267], comprising a 67 m-thick 

succession with ten lavas (Francis et al., 1970). 


in the northern Touch Hills, and north-eastern Gargunnock 

Hills, the basal macroporphyritic lava of the member is 

conformable or disconformable on a trachybasalt lava of 

the slackdown lava member. Farther west, where the 

trachybasalt is absent, the basal lava of the Baston Burn 

lava member is a transitional plagioclase-macrophyric 

to plagioclase-microphyric basalt, which overlies 

conformably or disconformably a microporphyritic basalt 

of the slackdown lava member. 

in the northern Touch Hills and north-eastern Gargunnock 

Hills, the Baston Burn lava member is overlain unconformably 

by the spout of Ballochleam lava member, and 

the Baston Burn lava member is progressively truncated 

towards the west. The lithological change is to microporphyritic 

basalt (‘Jedburgh’ type). in the north-western 

Gargunnock Hills, the Baston Burn lava member is 

overlain unconformably by the slackgun volcaniclastic 

member, and the lithological transition is to weathered 

basalt (bole) and well-bedded tuff. 

Thickness 

Between 9 and 67 m. in the extreme east [Ns 7315 9339 to 

7234 9297] the member is 15 m thick. it is thickest in the 

Gargunnock Burn [Ns 7073 9292 to 7060 9267]. 


The member is restricted to the northern part of the Fintry– 

Touch Block (Francis et al., 1970) and specifically to the 

northern Fintry Hills and the north-eastern Gargunnock 

Hills. These rocks crop out on a wide step in the 

escarpment above the cliffs formed by the slackdown 

lava member, extending north-east from the north side 

of lees Hill [Ns 6580 9120] to standmilane Craig [Ns 

670 918] and Black Craig [Ns 685 924] and east to the 

Gargunnock Burn [Ns 7073 9292 to 7060 9267] and 

Baston Burn [Ns 7351 9352]. 

Age 


4.3.3.57 slaCKgun volCaniClasTiC MeMBer 

Name 

previously named the slackgun interbasaltic Beds (see 

Francis et al., 1970). 

Lithology 

The slackgun volcaniclastic member consists predominantly 

of bedded tuff and/or volcaniclastic sedimentary rock, with 

weathered basalt lava (including bole) and a local olivinemicrophyric 

basalt lava.

Stratotype 

The type area is in the northern, western and south-western 

Fintry Hills, and the north-western Gargunnock Hills, northeast 

of Glasgow [Ns 6224 8636 to 6878 9241] (Francis et 

al., 1970). A reference section is the corrie-like scar of 

slackgun, immediately north-west of lees Hill, northern 

Fintry Hills [Ns 6576 9118 to 6577 9112] where Francis et 

al. (1970) recorded a partially obscured, 34 m-thick, section 

up the scarp. 


The slackgun volcaniclastic member unconformably 

overlies the skiddaw lava member. The lithological 

change is from transitional plagioclase-macrophyric to 

plagioclase-microphyric basalt lava or composite basalt 

lava to a dull red bole reflecting prolonged weathering of 

the underlying lavas. 

The slackgun volcaniclastic member is overlain, conformably 

or disconformably, by the spout of Ballochleam 

lava member. The lithological change is from tuff or 

volcaniclastic sedimentary rock to plagioclase-microphyric 

basalt lava (‘Jedburgh’ type). 

Thickness 



The member is restricted to the northern Fintry–Touch 

Block (Francis et al., 1970) and specifically to the Fintry 

Hills and the north-western Gargunnock Hills, north-east of 

Glasgow. These rocks crop out from north-east of spittalhill 

[Ns 6521 8669] to the west-north-west to below double 

Craigs [Ns 631 875], north-north-west to below stronend 

[Ns 626 895], and east-north-east to Black Craig [Ns 6878 

9241]. 

Age 


4.3.3.58 sPouT oF BalloCHleaM lava MeMBer 

Name 

previously named the spout of Ballochleam Group (see 


Lithology 

The spout of Ballochleam lava member consists 

predominantly of plagioclase-microphyric basalt lavas 

(‘Jedburgh’ type) and forms prominent crags. The lavas are 

comparatively impersistent and hard to correlate between 

adjacent sections, and some are divided into ‘flow-units’ 

(Francis et al., 1970). many of the basalt lavas have a 

relatively coarse grain size and are massive. The lavas are 

also variably slaggy, vesicular with sporadic amygdales, 

platy, and sporadically columnar jointed, and spheroidally 

weathered. Boles, some with nodules of decomposed lava, 

are developed on the tops of some lavas. The member also 

includes, near the base, rare olivine-microphyric basalt 

lavas (‘dalmeny’ type) [Ns 7061 9266], and higher within 

the member isolated plagioclase-macrophyric basalt lavas 

(‘markle’ type). North of scout Head [Ns 735 634] in the 

Touch Hills, the member comprises only three or four lavas, 

but farther west [Ns 7233 9297 to 7240 9276] it includes 

five or more lavas. At the Gargunnock Burn [Ns 7061 9266 

to 7064 9250] there are seven lavas. 

Stratotype 

The type area is in the northern and western Fintry Hills, 

and the northern Gargunnock and Touch hills, north-east 

49 

of Glasgow [Ns 6365 8701 to 7437 9374] (Francis et al., 

1970). A reference section is a gully in steep cliffs, east end 

of standmilane Craig, north-east Gargunnock Hills [Ns 6757 

9210 to 6762 9200] (Francis et al., 1970). Here the member is 

82 m thick, but contacts between units are generally obscured. 


in the northern Touch Hills and the north-eastern Gargunnock 

Hills, the basal plagioclase- or olivine-microphyric basalt 

lava of the member lies unconformably on the eroded 

plagioclase-macrophyric lavas of the Baston Burn lava 

member, progressively overstepping them to the west. in 

the north-western Gargunnock Hills and in the Fintry Hills, 

the member overlies, conformably or disconformably, tuffs 

of the slackgun volcaniclastic member. 

in the north and west Fintry Hills, the member is overlain, 

apparently conformably or disconformably, by the shelloch 

Burn lava member and the lithological change is to trachybasalt 

lava. in the northern Gargunnock Hills and north-western 

Touch Hills, however, the member is overlain, possibly disconformably, 

by trachybasalt lava of the lees Hill lava member 

and in the north-eastern Touch Hills, possibly disconformably, 

by the Gargunnock Hills lava member. in the latter case, the 

lithogical change is to plagioclase-macrophyric basalt lava. 

Thickness 

Between 24 and 91m. The member is of varible thickness, 

but generally thickens to the west. North of scout Head 

[Ns 735 634], in the Touch Hills, it is less than 30 m thick, 

but farther west [Ns 7233 9297 to 7240 9276] it is more 

than 50 m thick. in the Gargunnock Burn [Ns 7061 9266 to 

7064 9250] the member is about 45 m thick. The member is 

thickest, at more than 80 m, in the headwaters of the easter 

Blackspout [Ns 6912 9252 to 6911 9242]. 


The member is restricted to the Fintry–Touch Block (Francis 

et al., 1970) and specifically to the western and northern parts 

of the Fintry Hills, and the northern parts of the Gargunnock 

and Touch hills. These rocks crop out from the crest of 

the crags at double Craig [Ns 6365 8701], westwards 

to Ballmenoch Burn [Ns 6485 8692 to 6464 8752], and 

northwards to the prominent crags below stronend [Ns 6266 

8950] which extend eastwards to the spout of Ballochleam 

[Ns 6526 8998] and on to the north-north-east, below lees 

Hill [Ns 6587 9106] and east-north-east to standmilane 

Craig [Ns 6704 9176] and Black Craig [Ns 6841 9228]. 

From there, the outcrop continues to the east, passing through 

more crags and then to Baston Burn [Ns 7437 9374]. 

Age 


4.3.3.59 sTronenD volCaniClasTiC MeMBer 

Name 

previously known as the stronend interbasaltic Beds (see 


Lithology 

The stronend volcaniclastic member consists predominantly 

of volcaniclastic sedimentary rocks and possible tuff, with 

weathered basalt lava (including bole). it weathers back to 

form a prominent shelf in the escarpment on the western 

side of the Fintry Hills. 

Stratotype 

The type area is in the western Fintry Hills, north-east of 




1970). A reference section is 0.5 km south of stronend 

summit, western Fintry Hills [Ns 6288 8885] (Francis et al., 

1970). Here more than 1.5 m of bole lying near the base of 

the member is exposed. 


weathered basalt (bole) at the base of the member is 

conformable or disconformable on plagioclase-microphyric 

basalt lava of the spout of Ballochleam lava member within 

which the stronend volcaniclastic member is interdigitated. 

volcaniclastic rocks of the stronend volcaniclastic 

member are overlain by plagioclase-microphyric basalt 

lava of the spout of Ballochleam lava member, within 

which the stronend volcaniclastic member is interdigitated. 

Thickness 

uncertain. Francis et al. (1970) stated that the member 

seems to be relatively thin and local. At stronend summit 

[Ns 6288 8885] more than 1.5 m of bole is exposed, lying 

near the base of the member. in a tributary of Cammal 

Burn [Ns 6399 8764] more than 2.7 m of bole crops out, 

probably at the top of the member. 



(Francis et al., 1970) and specifically to the western Fintry 

Hills, north-east of Glasgow. These rocks crop out out in a 

restricted area from the western side of stronend [Ns 6274 

8953] to the south-south-east, to north of double Craig [Ns 

6322 8808]. 

Age 


4.3.3.60 lees Hill lava MeMBer 

Name 

previously named the lees Hill Group (Francis et al., 1970). 

Lithology 

The lees Hill lava member consists predominantly of 

trachybasalt but also includes a plagioclase-macrophyric 

basalt lava (‘markle’ type), and the rocks generally form 

the crest of the escarpment at the top of the cliffs formed by 

the spout of Ballochleam lava member. The trachybasalt is 

typically fine grained, massive, locally ‘slaggy’ and highly 

vesicular, and with local platy jointing. A single trachybasalt 

lava is present in the east [Ns 7184 9247], which occurs as 

an intercalation within the macroporphyritic basalt lavas 

of the Gargunnock Hills lava member, near to its base. in 

the Gargunnock Burn [Ns 7065 9249 to 7059 9222] two 

trachybasalt lavas are present, separated by a plagioclasemacrophyric 

basalt lava that is absent farther west, where 

the member consists entirely of trachybasalt lavas. 

Stratotype 

The type area is in the northern Gargunnock Hills and 

northern Touch Hills, north-east of Glasgow [Ns 6616 8971 

to 7184 9247] (Francis et al., 1970). A reference section is 

Gargunnock Burn, central northern Gargunnock Hills [Ns 

7065 9249 to 7059 9222] (Francis et al., 1970). Here the 

entire thickness (about 40 m) of the member exists and is 

largely exposed, though parts, including the top 1.5 m and 

basal 0.6 m, are obscured. 


The basal trachybasalt of the member lies possibly 

disconformably on plagioclase-microphyric basalt 

(‘Jedburgh’ type) of the spout of Ballochleam lava member. 



50 

in the east of its outcrop, the member is represented by a single 

trachybasalt lava that overlies, apparently conformably or 

disconformably, a plagioclase-macrophyric basalt (‘markle’ 

type) of the Gargunnock Hills lava member. 

The lees Hill lava member is overlain, apparently 

conformably or disconformably, by the Gargunnock Hills 

lava member, and in the east of its outcrop, the lees Hill 

lava member is represented by a single trachybasalt lava, 

which is intercalated with lavas of the Gargunnock Hills 

lava member. The lithological change is to plagioclasemacrophyric 

basalt lava (‘markle’ type). 

Thickness 

Between 0 and about 40 m 


The member is restricted to the northern part of the Fintry– 

Touch Block (Francis et al., 1970) and specifically to the 

northern Gargunnock Hills and northern Touch Hills, northeast 

of Glasgow. These rocks generally form the crest of the 

escarpment at the top of the cliffs formed by the spout of 

Ballochleam lava member and crop out northwards from 

Gourlay’s Burn [Ns 6628 8974 to 6625 9003] to lees Hill 

[Ns 660 910], east-north-east to standmilane Craig [Ns 

6722 9180] and Black Craig [Ns 6829 9219], and then 

eastwards through crags to the east of Gargunnock Burn 

[Ns 7195 9244]. 

Age 


4.3.3.61 sHelloCH Burn lava MeMBer 

Name 

previously named the shelloch Burn Group (Francis et al., 

1970). 

Lithology 

The shelloch Burn lava member consists of a varied 

assemblage of lavas including: trachybasalt that is variably 

massive to locally platy-jointed, slaggy and vesicular; basaltictrachyandesite 

(mugearite); plagioclase-microphyric 

basalt (‘Jedburgh’ type); plagioclase-macrophyric basalt 

(‘markle’ type); and transitional plagioclase-microphyric 

to plagioclase-macrophyric basalts. The member is best 

developed in the northern Fintry Hills and its upper 

part is well exposed in shelloch Burn [Ns 6509 8913 

to 6523 8924] where the sequence comprises a basaltictrachyandesite, 

a plagioclase-macrophyric basalt that is 

deeply weathered to a dull red bole basalt, and a basaltictrachyandesite 

(mugearite) that is deeply weathered to a 

dull red bole. The lower part of the member is best exposed 

in Boquhan Burn [Ns 6468 8967 to 6490 8963] where the 

sequence comprises a trachybasalt lava, which is deeply 

weathered to a dull red bole and a basaltic-trachandesite 

(mugearite). west of the Balmenoch Fault (Francis et al., 

1970) the member forms the highest part of the Fintry Hills 

but is not well exposed. However, a good section through 

all but the highest lavas in the member is seen in the 

highest of the crags that form the western edge of the Fintry 

Hills [Ns 6281 8910 to 6304 8870] where the sequence 

comprises a trachybasalt, two transitional plagioclasemacrophyric 

to plagioclase-microphyric basalts, another 

trachybasalt, two basaltic-trachyandesites (mugearites) and 

a further trachybasalt. 

Stratotype 

The type area is in the Fintry Hills, north-east of Glasgow 

[Ns 6361 8794 to 6489 8991] (Francis et al., 1970). A

eference section is in crags forming the western edge of 

the Fintry Hills [Ns 6281 8910 to 6304 8870] that shows 

all but the highest lavas in a section 60 m thick (Francis et 

al., 1970). The member is well exposed in shelloch Burn 

[Ns 6509 8913 to 6523 8924] where a section 21 m thick 

includes the top of the member. The lower part of the 

member, including its base, is best exposed in Boquhan 

Burn [Ns 6468 8967 to 6490 8963]. Here the section is 

18 m thick (Francis et al., 1970). 


The basal trachybasalt lava of the member is conformable or 

disconformable on the underlying plagioclase-microphyric 

basalts of the spout of Ballochleam lava member. 

The member is overlain unconformably by the Fintry 

Hills lava member. The lithological change is from basaltic-trachyandesite 

(mugearite) or trachybasalt to plagioclase-microphyric 

basalt. 

Thickness 

Between 40 and 61m 



et al., 1970), specifically to the Fintry Hills, north-east of 

Glasgow. These rocks crop out from around stronend [Ns 

6290 8946] in the north-west of the Fintry Hills towards 

the east, in the Boquhan Burn and its headwaters [Ns 6388 

8988 to 6490 8965] and the shalloch Burn [Ns 6513 8920 

to 6541 8939], and south-east to the Balmenoch Burn [Ns 

6465 8771 to 6464 8753] and beyond, although the limits of 

the member to the south-east are uncertain. 

Age 


4.3.3.62 FinTry Hills lava MeMBer 

Name 

previously named the Fintry Hills Group (see Francis et 

al., 1970). 

Lithology 

The Fintry Hills lava member consists predominantly of 

plagioclase-macrophyric basalt lavas (‘markle’ type) with a 

fairly high proportion of microporphyritic basalts and rare 

basaltic-trachyandesite (mugearite). Tuff occurs locally at 

[Ns 6409 8794]. 

Stratotype 

The type area is in the highest parts of the Fintry Hills, 

north-east of Glasgow [Ns 6369 8867 to 6321 8911] 

(Francis et al., 1970). 


The basal basalt of the member lies apparently conformably 

or disconformably on trachybasalt of the shelloch Burn 

lava member. The upper boundary is eroded but not 

exposed. 

Thickness 

more than 122 m. The top of the member is eroded. 



(Francis et al., 1970) and specifically to the Fintry Hills, 

north-east of Glasgow. These rocks crop out across the 

hilltops of the central part of the Fintry Hills [Ns 6369 8867 

to 6321 8911]. 

51 

Age 


4.3.3.63 CringaTe volCaniClasTiC MeMBer 

Name 

previously named the Cringate interbasaltic Beds (Francis 

et al., 1970). 

Lithology 

The Cringate volcaniclastic member consists of variably 

stratified volcaniclastic sedimentary rocks and/or tuffs. 

An exposure in the north-east bank of the endrick water 

at [Ns 6800 8750] shows poorly stratified dull red tuff 

or volcaniclastic sedimentary rock with persistent beds of 

red mudstone, interspersed with lenticular masses, up to 

1.5 m thick, of unsorted lava fragments set in a matrix of 

greenish clay. The fragments include decomposed basalt 

up to 20 cm across, commonly rounded but with irregular 

margins that seem to interlock. some are scoriaceous with 

small irregular amygdales filled with chlorite or carbonate 

minerals. The matrix includes carbonate minerals but also 

contains some grains of quartz and feldspar. 

Stratotype 

The type section is in the endrick water, between the Fintry 

Hills and the south-western Gargunnock Hills, north-east of 

Glasgow [Ns 678 879 to 682 873] (Francis et al., 1970). A 

reference section is in a left-bank tributary of the endrick 

water near Cringate [Ns 683 874 to 6858 8756]. 


in the endrick water at [Ns 6807 8742], the Cringate 

volcaniclastic member overlies highly decomposed 

microporphyritic basalt, thought to be roughly equivalent 

to middle parts of the spout of Ballochleam lava member 

(Francis et al., 1970). in a left-bank tributary of the 

endrick water at [Ns 6858 8756], about 40 m of tuff 

or volcaniclastic sedimentary rock is overlain by 6m of 

microporphyritic basalt that forms a waterfall (Francis et al., 

1970). The basalt is probably one of the highest lavas of the 

spout of Ballochleam lava member. 

Thickness 

At least 45 m 


The member is restricted to the Fintry-Touch Block (Francis 

et al., 1970) and specifically to the valley of the endrick 

water around Cringate [Ns 685 873], between the Fintry 

Hills and the south-western Gargunnock Hills, north-east 

of Glasgow. 

Age 


4.3.3.64 gargunnoCK Hills lava MeMBer 

Name 

previously named the Gargunnock Hills Group (Francis et 

al., 1970). 

Lithology 

The Gargunnock Hills lava member consists predominantly 

of plagioclase-macrophyric basalt (‘markle’ type) and 

composite lavas, with subordinate plagioclase-microphyric 

basalt (‘Jedburgh’ type) and rare basaltic-trachyandesite 

(mugearite) lavas. The topmost part of the member is well 

exposed in the gorge of the Touch Burn, downstream from 

the waterfall of Gilmour’s linn [Ns 7395 9252] where 



there are three massive to variably ‘slaggy’, plagioclasemacrophyric 

basalt lavas, with weathered tops (dark red boles 

with nodules of decomposed, ‘slaggy’ basalt). The remainder 

of the member is reasonably well exposed on the northern and 

eastern slopes of scout Head [Ns 7354 9337 to 7350 9313] 

where plagioclase-microphyric basalt lava flows (several of 

which are transitional to plagioclase-macrophyric basalt), and 

plagioclase-macrophyric basalt basalt lava flows are present. 

Stratotype 

The type area is in the Gargunnock and Touch hills, and the 

northern Kilsyth Hills, north-east of Glasgow [Ns 6970 8456 

to 7515 9360] (Francis et al., 1970). partial type sections occur 

in the Touch Burn [Ns 7395 9252] and on the northern and 

eastern slopes of scout Head, northern Touch Hills, north-east 

of Glasgow [Ns 7354 9337 to 7386 9301] (Francis et al., 1970). 

it is 75 m thick in all but the topmost flows of the member. 


in the northern Gargunnock Hills, the basal plagioclasemacrophyric 

basalt flow of the member lies, apparently 

disconformably, on trachybasalts of the lees Hill lava 

member. in the northern Touch Hills, the Gargunnock 

Hills lava member interdigitates with the lees Hill 

lava member and lies, probably disconformably, on 

microporphyritic basalts (‘Jedburgh’ type) of the spout 

of Ballochleam lava member. in the eastern part of the 

Kilsyth Hills, Campsie Block, the Gargunnock Hills lava 

member overlies the langhill lava member, but the nature 

of the contact is unknown. in the north-eastern Kilsyth Hills 

the member overlies, probably unconformably, the Campsie 

lava member. 

in the Gargunnock Hills and north-western Touch Hills, 

the member occupies the highest ground and its top is eroded. 

However, in the north-eastern and eastern Touch Hills, 

the member is overlain by the Black mount lava member. 

The change in lithology is from plagioclase-macrophyric 

basalt to plagioclase-microphyric basalts and subordinate 

basaltic trachyandesite (mugearite). 

Thickness 

From 91 m in the east, to more than 150 m in the west, 

where the top of the member is eroded. 



et al., 1970) and the north-eastern part of the Campsie Block 

(Forsyth et al., 1996) and specifically to the north-eastern 

Kilsyth Hills, and the Gargunnock and Touch hills, northeast 

of Glasgow. These rocks crop out in the north-eastern 

Kilsyth Hills on the upper parts of Cairnoch Hill [Ns 697 857], 

Craigannet Hill [Ns 712 848] and dundaff Hill [Ns 735 844] 

and over much of the area to the north of shielwalls Fault 

(Craig, 1980), including Craigengelt Hill [Ns 7240 6852], 

earl’s Hill [Ns 7175 8842] and Cringate law [Ns 6834 8830], 

and the area to the north, south and west of loch Coulter [Ns 

764 860]. The rocks also crop out extensively across the upper 

parts of the Gargunnock Hills, from Burnfoot [Ns 675 883] in 

the south-east, north-north-east to Carleatheran [Ns 6877 9186] 

and east, across the Touch Hills to Craigniven [Ns 7515 9360]. 

Age 


4.3.3.65 BlaCK MounT lava MeMBer 

Name 

previously named the Black mount Group (see Francis et 

al., 1970). 



52 

Lithology 

The Black mount lava member consists predominantly of 

plagioclase-microphyric basalt lavas (‘Jedburgh’ type) with 

subordinate basaltic-trachyandesite (mugearite) lavas. The 

microporphyritic basalt lavas are variably albitised, slaggy, 

vesicular, and platy-jointed and are locally transitional to a 

partly plagioclase-macrophyric lithology. 

Stratotype 

The type area is in the eastern Touch Hills, north-east of 


1970). The member is best exposed in the steep cliff that 

fringes the northern edge of Black mount [Ns 7436 9226] 

and forms the south side of the Touch Burn gorge [Ns 

7438 9244] where, in a reference section, it includes at least 

three microporphyritic basalt flows and a very fine-grained, 

platy-jointed, slaggy, basaltic-trachyandesite (mugearite). 

The section is 27 m thick and includes the base of the 

member (Francis et al., 1970). 


The basal plagioclase-microphyric basalt of the Black mount 

lava member is apparently conformable or disconformable 

on plagioclase-macrophyric basalt lava of the Gargunnock 

Hills lava member. 

The Black mount lava member is overlain by plagioclasemacrophyric 

basalt lava (‘markle’ type) of the Touch House 

lava member. The lithological transition is from plagioclasemicrophyric 

basalt to plagioclase-macrophyric basalt. 

Thickness 



The member is restricted to the north-eastern part of the 

Fintry–Touch Block (Francis et al., 1970) and specifically 

to the eastern Touch Hills, north-east of Glasgow. These 

rocks crop out from the west side of Black mount [Ns 7391 

9175] to near seton in the north-east [Ns 7600 9327] and 

Garter wood in the east [Ns 7652 9189]. 

Age 


4.3.3.66 TouCH House lava MeMBer 

Name 

previously named the Touch House Group (see Francis et 

al., 1970). 

Lithology 

The Touch House lava member consists only of plagioclasemacrophyric 

basalt or trachybasalt lavas (basalt to hawaiite 

of ‘markle’ type) and only the lowest part of the member 

is well exposed, near the edge of the low-lying fertile land 

between Touch Home Farm [Ns 7518 9331] and Touch 

House [Ns 7535 9276]. 

Stratotype 

The type area is in the eastern Touch Hills, north-east of 


1970). A reference section in the lowest part of the member 

is provided by exposures between Touch saw mill and 

Touch House, eastern Touch Hills, north-east of Glasgow 

[Ns 7518 9331 to 7535 9276]. 


The basal plagioclase-macrophyric basalt lava of the 

member is apparently conformable, or disconformable,

on the underlying plagioclase-microphyric basalt of the 

Black mount lava member. The top of the member is not 

exposed. 

Thickness 

uncertain. The thickness of the member is difficult to 

estimate because of drift cover, and the lack of knowledge 

about its upper part (Francis et al., 1970). 


The member is restricted to the north-eastern part of the 

Fintry–Touch Block (Francis et al., 1970) and specifically 

to a small area in the eastern Touch Hills, north-east of 

Glasgow. These rocks crop out in an outlier that extends 

northward from Touch House [Ns 7535 9276] to near 

Touch Home Farm [Ns 7524 9340] and westwards to north 

of mill linn [Ns 9495 9302]. 

Age 


AYR 

4.3.3.67 greenan CasTle PyroClasTiC MeMBer (gCP) 

Name 

The Greenan Castle pyroclastic member was previously 

known as ‘bedded agglomerate of Greenan Castle’ by eyles 

et al. (1949), and Greenan Castle Ash by whyte (1964). The 

present member was defined by williamson and monaghan 

in stephenson et al. (2002). see also sowerbutts (1999); 

whyte (1992). 

Lithology 

The member comprises bedded volcaniclastic coarse 

sandstone, with subsidiary lithic lapilli-tuffs and tuffs. 

Stratotype 

The type section is on the shore and in the cliff at Greenan 

Castle, south of Ayr [Ns 2311 6195 to 2313 6195], where 

the full thickness of the member is seen (see eyles et al., 

1949; whyte, 1964; 1992). 


where seen on the shore at Greenan Castle the lower 

boundary is possibly disconformable on sandstones, 

mudstones and ‘cementstones’ of the underlying Ballagan 

Formation (inverclyde Group). 

The upper boundary at the same locality is seen to pass 

upwards unconformably into mudstones and sandstones of 

the lawmuir Formation. 

Thickness 

some 23 m at Greenan Castle in the Ayr district, dying out 

laterally. 


A local unit on the shore and around Greenan Castle south of 

Ayr, which dies out about 1 km inland. it has been correlated 

on lithological grounds with the nearby Heads of Ayr vent. 

Age 

Chadian to Asbian 

4.3.4 Kirkwood Formation (KRW) 

Name 

Taken from Kirkwood Farm, strathclyde Region. The name 

was introduced by monro (1982). 

53 

Lithology 

The Kirkwood Formation consists of tuffaceous mudstones 

and tuffs, locally intercalated with non-tuffaceous 

sedimentary rocks, with some marine horizons developed. 

The tuffaceous mudstones and tuffs vary in colour from 

dark reddish brown to greenish grey. Non-tuffaceous 

sedimentary rocks, sandstones, siltstones and limestones, 

generally grey in colour, also occur within a restricted area 

intercalated with volcaniclastic rocks. 


The strata were largely formed by the reworking of materials 

derived from the underlying volcanic rocks but some primary 

ash-fall tuffs may be present. The formation shows extensive 

lateritisation, the product of a period of intense subaerial 

tropical weathering. There are some marine incursions. 

Stratotype 

The type section of the Kirkwood Formation occurs 

between 38.9 and 75.45 m depth in the Kirkwood Borehole 

(BGs Registration Number Ns34Ne/11) [Ns 3885 4716], 

near Kilmarnock (monro, 1999). This is the complete 

thickness of the formation at this locality. 


The base of the formation is taken at the lithological change 

from the underlying lavas of the Clyde plateau volcanic 

Formation into volcaniclastic sedimentary rocks (Figure 6, 

Column 4A). 

The top is generally taken at the base of the overlying 

mudstones, siltstones and sandstones of the lawmuir 

Formation or the cyclical limestones and clastic lithologies 

of the lower limestone Formation (Clackmannan Group). 

This boundary is commonly irregular and transitional with 

an interdigitation of lithologies. 

Thickness 

The Kirkwood Formation varies in thickness, from about 

6 to more than 41 m (monro, 1999, fig. 9) with thinning 

generally taking place towards the areas where the Clyde 

plateau volcanic Formation is thick. in the irvine district, 

monro (1999, p. 35, fig. 11) recorded a thickness of 

41.39 m encountered in the Coalhill No. 2 Borehole (BGs 

Registration Number Ns24Nw/20) [Ns 2432 4653] (a 

minimum thickness since the borehole did not reach the 

Clyde plateau volcanic Formation), and referred to localised 

thinning in boreholes close to the dusk water Fault. in the 

Kilmarnock district macpherson et al. (2000, p. 9) stated 

that the thickness of the formation averages around 15 m. 

BGs (1996) gave a generalised thickness of 18.75 m for the 

formation in the main coalfield area at machrihanish. 


western midland valley and machrihanish 

Age 

visean (Asbian to early Brigantian) (monro, 1999; Browne 

et al., 1999) 

4.3.5 Lawmuir Formation (LWM) 

Name 

Taken from lawmuir, strathclyde Region. The name was 

introduced by paterson and Hall (1986). 

Lithology 

The lawmuir Formation consists of a sequence of 

mudstones, siltstones and sandstones with seatrocks, coals 



and limestones. To the north of Glasgow around milngavie, 

the lower part is dominated by fluvial sandstones with a 

local development of quartz conglomerate. in the south of 

Glasgow around paisley, fluvial sandstones are interbedded 

with thick, poorly bedded siltstones and mudstones with 

a few thin coals. in one small area these coals coalesce 

to form a single seam 20 m thick. The upper part of the 

formation is partly arranged in cyclothems, with several 

marine incursions represented by marine limestones over 

a large area. A non-marine limestone (the Baldernock 

limestone) also occurs near the top of the sequence. 


Fluvial lower part becoming partly cyclothemic upwards 

with several marine incursions. 

Stratotype 

The type section of the lawmuir Formation (complete 

thickness) is between 11.75 and 266.2 m depth in the lawmuir 


5183 7310] west of Bearsden near Glasgow. 



change from the underlying volcaniclastic strata of the 

Kirkwood Formation into clastic sedimentary rocks. The 

boundary is commonly transitional, with interdigitation 

between sedimentary and volcaniclastic rocks. it can also 

rest directly on the lavas of the Clyde plateau volcanic 

Formation in the west of the midland valley of scotland 

(see paterson and Hall, 1986) (Figure 6, Columns 1, 4A) 

and on the apparently conformable but probably erosive 

surface of the characteristic mudstone, siltstone and ferroan 

dolostone lithologies of the Ballagan Formation (inverclyde 

Group) in Ayrshire (see monro, 1999, p. 39). 

The top of the lawmuir Formation is drawn at the base 

of the Hurlet limestone of the lower limestone Formation 

(Clackmannan Group). 

Thickness 

The maximum thickness of the formation is about 300 m 

in the Glasgow area. BGs (1987a) gave a generalised 

thickness of 185 m for the formation on the isle of Arran. 


western midland valley and the isle of Arran. The precise 

relationship between the lawmuir Formation and the 

pathhead Formation in Fife is not known because of a major 

geographical gap in information between the two areas. it 

is possible that the marine bands in the upper part of the 

lawmuir Formation are equivalent to all the marine bands 

in the pathhead Formation, in which case the nonmarine 

lower part of the lawmuir Formation would be equivalent 

to the sandy Craig Formation in Fife. 

Age 

visean (monro, 1999; Browne, 1999). 


see also Appendix 1. members of the lawmuir Formation 

in ascending stratigraphical order include: 

4.3.5.1 Douglas Muir QuarTz-CongloMeraTe MeMBer 

(DMQ) 

Name 

From douglas muir, strathclyde. see paterson and Hall 

(1986); Hall et al. (1998). 



54 

Lithology 

The douglas muir Quartz-Conglomerate member 

consists mainly of hard, white conglomerates with 

subordinate pebbly sandstones and a few lenses of 

purplish grey mudstone up to 30 cm thick. Trough 

cross-bedding is common in sets from 0.2–1.0 m thick. 

many of the units are upward-fining in grain size. The 

clasts and pebbles are almost exclusively of vein quartz 

and well rounded, averaging 2 cm, but up to 10 cm in 

diameter, with some blocks of sandstone up to 15 cm 

across also present. 


palaeocurrent directions indicate transport of the original 

sediment towards the south-south-west. 

Stratotype 

The type section is at the douglas muir Quarry in the 

type area at douglas muir [Ns 525 746], near milngavie, 

strathclyde where 20 m, being part of the member, are 

exposed. 


The base of the member is drawn at the base of the 

conglomerate of the douglas muir Quartz-Conglomerate 

where it rests apparently unconformably on volcaniclastic 

sediments of the Kirkwood Formation (Figure 6, Column 

4A), as seen at a natural exposure at [Ns 5307 7752]. 

The top of the member is transitional by upward passage 

by interbedding from conglomerate of the douglas muir 

Quartz-Conglomerate member to white and pale grey sandstone 

of the Craigmaddie muir sandstone member, as seen 

at a natural exposure at [Ns 5730 7774]. 

Thickness 

incomplete thickness of 20 m at the type locality at douglas 

muir Quarry and up to 70 m maximum elsewhere. 


strathclyde. North of the River Clyde and eastwards from 

the the type area at douglas muir [Ns 525 746] to the site 

of the strathblane–Balmore Tunnel No. 8 Borehole (BGs 

Registration Number Ns57Ne/28) [Ns 5712 7731], but 

not in the adjacent parts of 1:50 000 scale Geological sheet 

31w (Airdrie). 

Age 

late visean (Asbian?) 

4.3.5.2 CraigMaDDie Muir sanDsTone MeMBer (CrMs) 

Name 

The member was previously named the Craigmaddie 

sandstone Formation by Tait (1973), and the Craigmaddie 

sandstones (of the upper sedimentary Group, Calciferous 

sandstone series) by Clough et al. (1925). 

Lithology 

sandstone, white, cross bedded, with pebbly ‘bands’ (beds) 

in places. locally, interbedded with mudstone and rare 

intercalations of volcanic detritus. strata within the member 

were described by Tait (1973) as fine-grained, buffweathering 

quartz arenite with conglomerate lenses that 

consist mainly of mudstone intraclasts. 


Tait (1973) interpreted the sandstone member as the 

deposits of a meandering river system.

Stratotype 

partial type sections were described by Hall et al. (1998), 

who referred to the prominent outcrops of bedrock on 

Craigmaddie muir exposing strata from the base and the 

middle parts of the member [Ns 580 766 to 588 764]. The 

type section of the upper part of the member (about 68 

m thick), to its upper boundary placed at the base of the 

Balmore marine Band, is recorded from exposures in the 

subsurface beneath Craigmaddie muir in the strathblane– 

Balmore tunnel (BGs Registration Number Ns57Ne/30) 

[Ns 5895 7521]. 


The lower boundary of the Craigmaddie muir sandstone 

member is mapped on Craigmaddie muir [Ns 5820 7652] 

and muirhouse muir [Ns 5723 7785] and placed where 

sandstones without interbeds of conglomerate are observed 

at outcrop (BGs, 1987b; see also BGs, 1987c). The 

underlying douglas muir Quartz-Conglomerate member 

is typically conglomerate with sandstone interbeds and, 

toward the top of the member, sandstone with pebbles 

or conglomerate beds (Figure 6, Column 4A). The lower 

boundary of the Craigmaddie muir sandstone member had 

previously been mapped slightly lower in the sequence by 

Tait (1973) who noted it to be gradational containing ‘lenses 

of conglomerate of similar composition’ to the underlying 

douglas muir Quartz-Conglomerate member near the base. 

The upper boundary of the Craigmaddie muir sandstone 

is placed at the base of the Balmore marine Band (Hall 

et al., 1998, fig. 9). This is at a higher position than that 

of Clough et al. (1925, fig. 2) who placed it at the top of 

the main sequence of sandstones about 45 m below the 

Craigenglen Beds, but at a lower position than Tait (1973) 

who placed the boundary beneath the Balgrochan Beds. 

Tait’s (1973) informal division ‘lower Craigmaddie muir 

sandstone member’ equates with the Craigmaddie muir 

sandstone member as presented here. 

Thickness 



The member is confined to the fault-bounded block south of 

the Craigend and Campsie faults and north of the Bankend 

and Glorat faults, extending from muirhouse muir [Ns 576 

777] eastwards to Craigmaddie muir [Ns 590 765], Craigend 

muir [Ns 585 776], and the vicinity of lennoxtown [Ns 626 

780], north-east of milngavie, strathclyde. 


visean (?Asbian–Brigantian). The Balmore marine Band 

immediately above the Cragmaddie muir sandstone 

member has a relatively sparse fauna including brachiopods. 

Correlatives of this bed contain the bivalve Posidonia becheri, 

which is thought to be of p 1b or p 1c age (Hall et al., 1998). 

FIFE (Figure 6, Column 4C) 

4.3.6 Fife Ness Formation (FNB) 

Name 

From Fife Ness, east Fife. The unit was originally described 

by Forsyth and Chisholm (1977) and first given formation 

status by Browne (1986). 

Lithology 

The Fife Ness Formation consists dominantly of off-white 

and reddish brown or purplish grey sandstone arranged in 

55 

upward-fining cycles. Argillaceous beds are commonly 

poorly bedded and seatearths are present, but there are no 

coal seams. Bedded dolostone is rare and the associated 

nonmarine faunas comprise ostracods, spirorbids and algal 

nodules. marine strata are absent. 


The formation is essentially fluvial and lacustrine in origin. 

Stratotype 

The type sections are those on the Fife coast at Fluke dub [No 

6228 1061 to 6205 1071] and at Fife Ness [No 6328 1014 to 

636 054]. The Fluke dub section includes some 60–90 m of 

alternating sandstone and grey mudstone with a few thin beds 

of bedded carbonate (one containing ostracods) from the base 

of the formation to the wormistone Fault. The Fife Ness section 

(which does not appear to overlap with that at Fluke dub) runs 

from the eastern margin [No 6328 1014] of a cryptovolcanic 

disturbance near Constantine’s Cave, round Fife Ness to the 

dane’s dike Fault. it includes about 180 m of mainly thick 

white sandstones with grey and red mudstones and some 

siltstones. Four beds of dolomite occur with faunas of Spirorbis 

sp., ostracods and fish remains. Algal material is present in one 

bed at [No 6358 1015] (Forsyth and Chisholm, 1977). 


in east Fife, the conformable base of the Fife Ness 

Formation lies in a lithological transition and is taken above 

the highest bed of carbonate conglomerate in the Clyde 

sandstone Formation of the Fluke dub section. The top is 

faulted against the Anstruther Formation in the Fife Ness 

type section (see Browne et al., 1999, fig. 2.19). 

Thickness 

The maximum thickness of the formation exceeds 230 m in 

east Fife (Forsyth and Chisholm, 1977, table 1). 


Fife 

Age 

early visean 

4.3.7 Anstruther Formation (ARBS) 

Name 

From Anstruther, east Fife. The unit was originally described 

by Forsyth and Chisholm (1977) and first given formation 

status by Browne (1986). 

Lithology 

The Anstruther Formation consists dominantly of 

mudstone, siltstone and sandstone in thin upwardcoarsening 

cycles. Nonmarine limestone and dolostone 

are also developed, usually as thin beds, some of which 

contain oncolites and stromatolites. minor components 

include marine mudstone and siltstone and a few algalrich 

oil-shale beds. sandstone, generally off-white 

and fine- to medium-grained, is subordinate to the 

argillaceous rocks, but thick, upward-fining, multistorey 

sandstones are locally developed. Thin beds of coal and 

ironstone are present. The formation is distinguished 

from the Fife Ness Formation, below, by the lower 

proportion of sandstone in it, and from the overlying 

pittenweem Formation by the relative paucity of its 

marine faunas. locally, basalt lavas and lapilli-tuff of the 

Charles Hill volcanic member are present at the base of 

the formation. 




The pattern of sedimentation is of upward-coarsening 

lake-delta cycles, with thinner upward-fining fluvial units 

erosively capping them, and minor marine incursions. 

Stratotype 

partial type sections in the Anstruther Formation occur on 

the Fife coast at Anstruther wester [No 5670 0310 to 5635 

0300], at Billow Ness [No 5590 0269] and at Cuniger Rock 

[No 5598 0265 to 5566 0271]. A representative section 

was cored in the Anstruther Borehole (BGs Registration 

Number No50se/5) [No 5653 0350]. 


The base of the formation is not known at outcrop in east 

Fife but would be taken at the lithological change from 

sandstone-dominated sequences of the underlying Fife Ness 

Formation into mudstone-rich cyclical deposits. The top is 

drawn at the base of the Cuniger Rock marine Band at the 

base of the pittenweem Formation (see Browne et al., 1999, 

fig. 2.19). 

Thickness 

The maximum thickness of the formation exceeds 810 m 

(Forsyth and Chisholm, 1977, table 1). 


Fife 


visean. The marine faunas are usually restricted. The 

abundant but restricted nonmarine faunas are dominated by 

Naiadites obesus, with Paracarbonicola in the lower part 

of the formation. 


see also Appendix 1. member of the Anstruther Formation: 

4.3.7.1 CHarles Hill volCaniC MeMBer (CHvo) 

Name 

From Charles Hill, Fife. previously known as the Charles 

Hill volcanic Beds. see Browne et al. (1987); Browne et 

al. (1999). 

Lithology 

The Charles Hill volcanic member consists of pale greenish 

grey to grey, amygdaloidal, earthy, weathered to hard 

olivine-microphyric basalt (‘dalmeny’ type) lavas and beds 

of grey and pink ash-fall and/or waterlain lapilli-tuff. Beds 

of limestone and mudstone are known very locally (as on 

the island of meadulse). 

Stratotype 

The type area is on Charles Hill at Barnhill Bay [NT 1860 

8380 to 1850 8365] near Aberdour in Fife where more 

than 30 m of beds of lava and volcaniclastic rocks are 

seen (see Browne et al., 1987, fig. 15; Browne et al., 1999, 

fig. 2:18). Reference sections are also seen in the Firth 

of Forth on the islands of Craigdimas [NT 1920 8400], 

meadulse [NT 1895 8305], Car Craig [NT 1985 8305] 

and on the western shore and in skerries off inchcolm [NT 

185 824]. 


The lower boundary is defined at the base of the lowest lava 

or bed of volcaniclastic rock resting on noncyclic fluvial 

and lacustrine sedimentary rocks of the underlying Fife 

Ness Formation that consists of sandstones and mudstones 



56 

with beds of carbonate rock (limestone and dolostone) 

(Figure 6, Column 4C). This contact is nowhere seen and 

therefore may be transitional, sharp or unconformable. 

The top of the member is defined by the highest tuff bed 

that is overlain by the noncyclic sedimentary rocks of the 

overlying Anstruther Formation consisting of dark grey to 

black lacustrine mudstones with thin beds of argillaceous 

ostracod-bearing limestone and dolostone and pale grey 

sandstone. 

Thickness 

Tens of metres but very uncertain. Assessed as more than 

30 m thick at Charles Hill. 


Known at Aberdour on the Fife coast, and on various 

islands in the Firth of Forth. volcanic rocks, now no longer 

exposed at silverknowes [NT 205 776] on the shore at 

Granton–Cramond, edinburgh have also been assigned to 

the Charles Hill volcanic member, here interbedded with 

the Gullane Formation. This outcrop of basaltic lavas and 

tuffs, once quarried on the coastline, extends the supposed 

occurrence of the member across the inchkeith Fault and 

intercalating it with the ‘Abbeyhill shales Beds’ (Gullane 

Formation). 

Age 

Asbian. 

4.3.8 Pittenweem Formation (PMB) 

Name 

From pittenweem, east Fife. The unit was originally 

described by Forsyth and Chisholm (1977) and given 

formation status by Browne (1986). 

Lithology 

The pittenweem Formation consists dominantly of 

mudstone and siltstone. Beds of nonmarine limestone 

and dolostone are less common than in the Anstruther 

Formation. marine mudstone (including ‘marine bands’), 

siltstone and limestone occur as minor, but important, 

components. A few algal-rich oil-shale beds are also 

present. Generally fine- to medium-grained sandstone is 

subordinate to the argillaceous rocks, but locally thick, 

upward-fining, multistorey sandstones occur as well as thin 

beds of coal and ironstone. The formation is distinguished 

from those adjacent to it by the comparative diversity of the 

marine faunas, which probably all belong to the macgregor 

marine Bands (see Browne et al. 1999, p.10, table 3). 


The pattern of sedimentation is of upward-coarsening 

deltaic cycles, with thinner upward-fining fluvial units 

erosively capping them, and minor marine incursions. 

Stratotype 

Type sections in the pittenweem Formation occur on the 

shore near pittenweem at Cuniger Rock (basal contact) [No 

5566 0271 to 5510 0249] and from 700 m (top contact) 

to 830 m depth in the Kilconquhar Bore No. 79/1 (BGs 

Registration Number No40se/26) [No 4845 0305] near 

elie. A good section of the full succession is also exposed 

on the shore at st Andrews [No 506 173 to 513 169]. 


The conformable base of the pittenweem Formation lies 

in a transitional sequence, and is drawn at the base of the

Cuniger Rock marine Band above the mudstone, siltstone 

and sandstone of the Anstruther Formation (Figure 6, 

Column 4C). 

The top of the formation is at the top of the st Andrews 

Castle marine Band (sCmB), which is overlain by mudstone 

and siltstone of the sandy Craig Formation. 

Thickness 

The maximum thickness of the formation is now known to 

be more than 260 m in east Fife based on its development 

in the partial type sections (see above). Forsyth and 

Chisholm (1977, table 1) state that the formation is over 

220 m thick. 


Fife 


visean (Asbian). The marine faunas, which occur in 

thin ‘marine bands’, are usually diverse and sometimes 

abundant. The abundant but restricted nonmarine faunas are 

dominated by the bivalve Naiadites obesus. 

4.3.9 Sandy Craig Formation (SCB) 

Name 

From sandy Craig, east Fife. The unit was originally 

described by Forsyth and Chisholm (1977) and given 

formation status by Browne (1986). 

Lithology 

The sandy Craig Formation is characterised by mudstone 

and siltstone with a minor percentage of algal rich oil 

shale. Thin beds of non-marine limestone and dolostone 

are also developed, some of which contain oncolites and 

stromatolites. The Burdiehouse limestone of the lothians 

is represented in central Fife by at least three beds of 

limestone (Geikie, 1900, p. 46). multicoloured, mainly 

fine- to medium-grained sandstone is subordinate to the 

argillaceous rocks, but thick, upward-fining, multi-storey 

sandstones are locally developed. Greenish grey clayrock 

and calcareous mudstone occur, as do thin beds of coal 

and ironstone. Nodular beds of pedogenic limestone and 

dolomite (‘cornstone’) are also present. The formation is 

distinguished from its neighbours by the relative rarity of 

marine beds, and by the local presence of cornstones. 


The pattern of sedimentation within the formation is of upwardcoarsening 

deltaic cycles, with thinner upward-fining fluvial 

units erosively capping them, and rare marine incursions. 

Stratotype 

partial type sections in the sandy Craig Formation occur at 

pittenweem Harbour [No 5518 0236 to 5452 0238], nearby 

at sandy Craig [No 5453 0215 to 5419 0226] and from 203 to 

700 m depth in the Kilconquhar Bore 79/1 (BGs Registration 

Number No40se/26) [No 4845 0305] near elie. 


The conformable base of the sandy Craig Formation 

lies in a transitional sequence and is taken at the top 

of the st Andrews Castle marine Band (sCmB) above 

the mudstone and siltstone of the pittenweem Formation 

(Figure 6, Column 4C). 

The top of the formation is now drawn at the base of the 

west Braes marine Band (wBmB) (Browne, 1986, fig. 2), 

marking the base of the pathhead Formation. 

57 

Thickness 

The maximum thickness of the formation as now defined is 

about 670 m in east Fife (Browne, 1986, fig. 2). 


Fife 


visean (Asbian). marine faunas are very rare, and are 

usually restricted, consisting in some cases only of the 

brachiopod Lingula. The bivalve Curvirimula dominates 

the abundant, but restricted, nonmarine faunas. 

4.3.10 Pathhead Formation (PDB) 

Name 

From pathhead, east Fife. The unit was originally described 

by Forsyth and Chisholm (1977) and given formation status 

by Browne (1986). 

Lithology 

The pathhead Formation consists predominantly of mudstone 

and siltstone with beds of limestone and dolostone. pale 

coloured, fine- to medium-grained sandstone is subordinate 

to the argillaceous rocks. Thin beds of coal and ironstone 

also occur. 


The overall pattern of sedimentation within the formation is 

of upward-coarsening deltaic cycles, with thinner upwardfining 

fluvial units erosively capping them, and relatively 

common marine incursions. 

Stratotype 

The type section is on the coast at pathhead [No 5419 0226 

to 5381 0212] between st monans and pittenweem. 


The conformable base of the formation lies in a transitional 

sequence, the boundary being drawn at the base of the 

west Braes marine Band (wBmB) above the sandy Craig 

Formation (Figure 6, Column 4C), stratigraphically a little 

higher (Browne, 1986, fig. 2) than that originally described 

by Forsyth and Chisholm (1977). 

The top of the formation is at the base of the Hurlet 

limestone, present at the base of the lower limestone 

Formation (Clackmannan Group). 

Thickness 


(Browne, 1986, fig. 2). 


Fife 


visean (Brigantian). marine bands are more common than in 

the underlying formations and their faunas are usually diverse 

and abundant. Curvirimula dominates the nonmarine faunas. 

WEST LOTHIAN AND EDINBURGH (Figure 6, 

Column 4D): 

4.3.11 Arthur’s Seat Volcanic Formation (ASV) 

Name 

From Arthur’s seat, edinburgh. The formation name was 

established by Chisholm et al. (1989). 



Lithology 

The Arthur’s seat volcanic Formation consists of lavas, 

tuffs and volcaniclastic sedimentary rocks. The lavas are 

mildly alkaline and show a limited range of composition. 

The basic rocks are silica-undersaturated. They are 

macroporphyritic in the range olivine-pyroxene-phyric 

basalt and basanite–olivine-clinopyroxene-plagioclasephyric 

basalt–plagioclase-phyric hawaiite–mugearite. 


The formation was produced by one short-lived episode 

of volcanic activity. The depositional environment was 

terrestrial, probably on a coastal plain. 

Stratotype 

The type area is in Holyrood park, edinburgh [NT 28 73], 

but the natural sections here are incomplete. 


The base of the formation, though nowhere exposed or 

seen in boreholes, is considered to occur at a lithological 

change from underlying clastic sedimentary rocks of the 

Ballagan Formation (inverclyde Group) to lavas, tuffs 

or volcaniclastic sedimentary rocks of the Arthur’s seat 

volcanic Formation. 

The top of the formation, a presumed transition to the 

sedimentary lithologies of the Gullane Formation, is likewise 

concealed (Figure 6, Column 4d). 

Thickness 

The maximum thickness may be in excess of 300 m 

(mitchell and mykura, 1962, p. 43). 


lothians. The main outcrop is in Holyrood park, edinburgh 

with a faulted block on Calton Hill. The Craiglockhart Hills 

in edinburgh may be a faulted outlier of the same rocks. 

volcanic rocks at Corston Hill, Torweaving Hill, Black 

Hill, Harperrig, Buteland Hill and Cock Burn may belong 

to the same eruptive episode. other smaller separated 

outcrops are correlated with the Arthur’s seat volcanic 

Formation (see Browne et al., 1999). A confidential 

borehole at d’Arcy in the midlothian Coalfield may have 

proved an eastward extension of the formation, though this 

lithostratigraphical unit should now be referred to as the 

Garleton Hills volcanic Formation (m A e Browne, verbal 

communication, 01 march 2007). 

Age 

Chadian to Arundian. 

4.3.12 Gullane Formation (GUL) 

Name 

From Gullane, east lothian. The formation name was 


Lithology 

The Gullane Formation consists of a cyclical sequence 

predominantly of pale, fine- to coarse-grained sandstone 

interbedded with grey mudstone and siltstone. subordinate 

lithologies are coal, seatrock, ostracod-rich limestone/ 

dolostone, sideritic ironstone and rarely, marine beds with 

restricted faunas. 


The depositional environment was predominantly fluviodeltaic, 

into lakes that only occasionally became marine. 



58 

Stratotype 

The type section is from 155.44 to 287.27 m depth in 

the spilmersford Borehole (BGs Registration Number 

NT46Ne/73) [NT 4570 6902]. The formation is also 

notably recorded from 47.93 to 197.94 m depth in 

the Birnieknowes Borehole (BGs Registration Number 

NT77se/9) [NT 7580 7317] and on the coast at Cove (see 

Browne et al., 1999, fig. 2, col. 12) near Cockburnspath 

[NT 79 71] in the oldhamstocks Basin (lagios, 1983; 

Andrews and Nabi, 1994; see also Browne et al., 1999, 

p. 12). 


The base of the formation is taken at the top of the Garleton 

Hills or Arthur’s seat volcanic formations, where present 

(Figure 6, Columns 4d, e). where volcanic rocks are 

absent, it is taken at the lowest coal, or carbonaceous, or 

rooty beds above strata consisting predominantly of white 

sandstone with pedogenic limestone of the Clyde sandstone 

Formation (inverclyde Group). 

The top of the formation is drawn at the base of the 

macgregor marine Bands (wilson, 1989), located at the 

base of the west lothian oil-shale and Aberlady formations. 

Thickness 

The estimated maximum thickness of the formation is about 

560 m in west lothian (see Browne et al. 1999, fig. 2, 

col. 8; mitchell and mykura, 1962, fig. 9). 


lothians. 


visean, mainly TC miospore Zone of Neves et al. (1973; 

see also Chisholm et al., 1989; Chisholm and Brand, 

1994). 

4.3.13 West Lothian Oil-Shale Formation (WLO) 

Name 

The formation name was established by Chisholm et al. (1989). 

Lithology 

The west lothian oil-shale Formation is characterised by 

seams of oil shale in a cyclical sequence predominantly of 

pale coloured sandstones interbedded with grey siltstones 

and mudstones. subordinate lithologies are coal, ostracodrich 

limestone/dolostone, sideritic ironstone and marine 

beds, including bioclastic limestones with rich and 

relatively diverse faunas. Thick pale green-grey or grey 

argillaceous beds supposedly containing derived volcanicdetrital 

calcareous mudstone are present. 


The environment of deposition was similar to that of the 

Aberlady Formation, but with oil shales formed in large 

freshwater lakes, rich in algae and other organic matter. 

Stratotype 

The type area is west lothian, where a composite section 

of the formation has been built up from numerous boreholes 

drilled to prove the oil-shale seams. The base is well exposed 

in the water of leith near Redhall in edinburgh (see 

Chisholm and Brand, 1994, p. 100, localities 1–4; Browne 

et al., 1999, fig. 2, col. 9). most parts of the formation are 

partly exposed on the coast from south Queensferry to 

Blackness [NT 13 78 to 05 80].


The base of the formation is taken at the base of the 

Humbie marine Band, the local equivalent of the 

lowest macgregor marine Band and is underlain by the 

predominantly sandstone, mudstone and siltstone of the 

Gullane Formation (Figure 6, Column 4d). The formation 

is laterally equivalent to the Aberlady Formation to the 

east, and to the Kinghorn volcanic Formation to the north. 

it is also laterally equivalent to part of the Bathgate Hills 

volcanic Formation to the west. 

The top of the formation is drawn at the base of 

the Hurlet limestone, located at the base of the lower 

limestone Formation (Clackmannan Group). 

Thickness 

The maximum thickness of the formation is in excess of 

1120 m in west lothian (see Browne et al., 1999; Chisholm 

et al., 1989, section 4.5). 


lothians 


visean (Asbian to Brigantian). miospores of the TC, Nm 

and vF zones of Neves et al. (1973) are represented. The 

macgregor marine bands at the base of the formation 

have rich and distinctive faunas including Punctospirifer 

scabricosta, Pteronites angustatus and Streblopteria 

redesdalensis. wilson (1952) described the B Zone 

ammonoid Beyrichoceratoides redesdalensis from the Cove 

lower marine Band, but this bed cannot be correlated with 

certainty with the Humbie marine Band at the base of the 

Gullane Formation. The Granton ‘shrimp-bed’ within the 

formation on the shore north of edinburgh is the locality 

where the soft structures of a conodont animal were first 

described (Briggs et al., 1983). 


see also Appendix 1. members of the west lothian oilshale 

Formation in stratigraphical order include: 

4.3.13.1 CalDers MeMBer (CDe) 

Name 

The name was proposed by Chisholm et al. (1989), the main 

outcrop area and the thickest development of the member 

being around west Calder, midcalder and east Calder. 

Lithology 

The Calders member comprises a succession of black to 

grey mudstones, grey siltstones and white, grey and pink 

sandstones with thin beds of grey argillaceous, limestone 

and dolostone (‘cementstone’), and algal-rich black to grey 

oil shales with some lapilli-tuff beds. The strata are not 

disposed in readily recognisable sedimentary cycles. The 

member includes the dalmahoy oil-shale, Hailes sandstone 

(which was much worked in the past for dimension stone), 

pumpherston shell Bed (a bed of fossiliferous mudstone with 

a marine fauna), and the overlying pumpherston oil-shale. A 

regionally persistent but thin (less than 1 m) algal dolostone 

has been recognised at Hopetoun and Queensferry. 


The strata are almost all of lacustrine and fluvial origins, 

with sporadic marine incursions. 

Stratotype 

The type section is the shore at Queensferry between 

longcraig pier [NT 144 786] and just east of the Forth 

59 

Railway Bridge [NT 138 784] (Carruthers et al., 1927 

p. 80; mcAdam and Clarkson, 1986, map 24). Reference 

sections include the shore and coastal section at Hopetoun 

[NT 088 793 to 094 791] (Carruthers et al., 1927), and 

the river section in the water of leith near Redhall in 

edinburgh [NT 217 702 to 214 697] (Chisholm and Brand, 

1994, p. 100), which exposes the Redhall marine Band and 

overlying mudstones with oil-shales, up to the base of the 

Hailes sandstone. 


The lower boundary is defined by the Redhall (Humbie) 

marine Band. This is the lowest of the macgregor marine 

Bands in the area, up to 0.3 m thick, and in edinburgh 

is contained within at least 13.8 m of generally tough, 

black and dark grey mudstones. The lowest 9 m of these 

mudstones form the top of the underlying Gullane Formation 

(Chisholm and Brand, 1994, p. 100) which are assigned to 

the currently undefined wardie shales member. 

The top of the Calders member is defined at the base of 

the Burdiehouse limestone (Buls) (mitchell and mykura, 

1962, p. 67) (Figure 6, Column 4d). 

Thickness 

The member is on average about 290 m thick (Cameron 

and mcAdam, 1978, fig. 2) but estimated at 350 m in west 

edinburgh. The Hailes sandstone has a maximum thickness 

of about 57 m. 


west lothian and part of midlothian. The unit is no longer 

mapped as Calders member in Fife, where it is now mapped 

as the sandy Craig Formation (Figure 6, Column 4C). 


Asbian. Currie (1954) listed ammonoids from the 

pumpherston shell Bed including Beyrichoceratoides aff. 

fournieri, B. cf. fournieri or B. cf. redesdalensis, B. 

cf. truncatus and ?Dimorphoceras sp. on the evidence 

available Currie (1954) and George et al. (1976) assigned 

the pumpherston shell Bed to the middle visean (Asbian). 

4.3.13.2 HoPeToun MeMBer (Hon) 

Name 

The name was proposed by Chisholm et al. (1989) to replace 

the upper oil shale Group of Carruthers et al. (1927) and 

mitchell and mykura (1962). it originates from the best 

natural sections, which are on the coast near Hopetoun House. 

Lithology 

The Hopetoun member consists of a sequence of black 

to grey mudstone, grey siltstone, white, grey and pink 

sandstone and white to pale greenish grey calcareous 

mudstone with thin beds of black to grey oil shale, 

coals (Hurlet, Two Foot and Houston seams); together 

with grey to white, pure to argillaceous limestone and 

dolostone that comprise the upper part of the west 

lothian oil-shale Formation. some lapilli-tuff beds are 

present and thin coal seams. The strata are not generally 

disposed in readily recognisable sedimentary cycles. The 

member includes the Camps, under dunnet, dunnet, 

Broxburn, Fells, Grey, mungle, Raeburn and Fraser 

shales (oil shales), and the dunnet and Binny sandstones 

that were worked in the past for dimension stone. The 

limited number of thin marine beds include the dunnet, 

Raeburn and Fraser shell beds (fossiliferous mudstone 

beds with a marine fauna) and the under or Gilmerton 

Bone Bed limestone. lacustrine limestones are present 



such as the Barracks limestone with the regionally 

important and thick Burdiehouse limestone at the base 

of the member. The Bathgate Hills volcanic Formation 

(Bathgate Group) basaltic lavas and tuffs are interbedded 

near the top in the west lothian and Falkirk areas. The 

Hurlet Coal is the topmost named bed in the member in 

west lothian. 


The strata are almost all of lacustrine and fluvial origins 

with a limited number of marine incursions. 

Stratotype 

The shore at Abercorn [NT 061 794 to 088 793] provides 

a partial type section of limited exposure and modest 

quality. it includes from the Raeburn shale downwards. 

Reference sections occur on the shore at Queensferry [NT 

127 784] to port edgar [NT 138 784] (basal part of the 

member) and in the River Almond valley at mid Calder, 

west lothian [NT 079 671 to 086 685] (from the Broxburn 

shale downwards). 


The lower boundary is defined at the base of the 

Burdiehouse limestone (Buls) (mitchell and mykura, 

1962, p. 67) (Figure 6, Column 4d) resting on strata of the 

Calders member. This distinctive limestone is a lacustrine 

deposit, commonly 6–9 m thick, containing abundant 

fossilised ostracod, plant and fish remains, and rarely algal 

oncoids. 

The top of the generally noncyclic Hopetoun member 

is defined at the base of the Hurlet limestone (Figure 6, 

Column 4d). This marine limestone forms the base of 

the marine-dominated cyclic successions of the overlying 

lower limestone Formation (Clackmannan Group). 

Thickness 

The member is on average about 830 m thick in the 

lothians (Cameron and mcAdam, 1978, fig. 2). 


west lothian and part of midlothian. 

Age 

Asbian to Brigantian 

EAST LOTHIAN (Figure 6, Column 4E) 

4.3.14 Garleton Hills Volcanic Formation (GHV) 

Name 

From the Garleton Hills, east lothian. The formation name 

was established by Chisholm et al. (1989). 

Lithology 

The Garleton Hills volcanic Formation consists of lavas, 

tuffs and subordinate volcaniclastic sedimentary rocks. 

The lavas are transitional to mildly alkaline and show 

a limited range of composition. The basic rocks are 

hypersthene-normative. They are macroporhyritic in the 

range olivine-pyroxene-phyric basalt and basanite–olivineclinopyroxene-plagioclase-phyric 

basalt–plagioclase-phyric 

hawaiite–mugearite–trachyte. 


The formation was produced by a single episode of volcanic 

activity. The depositional environment was terrestrial, 

probably on a coastal plain. 



60 

Stratotype 

The type area is the Garleton Hills [NT 54 85], where there 

are many natural exposures. A reference section of thinner 

development occurs from 287.27 to 554.19 m depth in the 

spilmersford Borehole, south-west of Haddington (BGs 

Registration Number NT46Ne/73) [NT 4570 6902]. 



change from underlying clastic sedimentary rocks of the 

Ballagan Formation (inverclyde Group) to lavas, tuffs or 

volcaniclastic sedimentary rocks. This is gradational, and 

drawn where volcanic rocks predominate over sedimentary 

as in the spilmersford Borehole (see above). 

The top of the formation, at the base of the overlying 

Gullane Formation (Figure 6, Column 4e), is also gradational 

(as in the spilmersford Borehole). 

Thickness 

The maximum thickness of the formation may be about 

380 m (mcAdam and Tulloch, 1985, fig. 18). 


lothians. The rocks crop out in a belt from North Berwick 

to dirleton on the coast to the dunbar–Gifford Fault east of 

Haddington with their main outcrop in the Garleton Hills. A 

further outcrop occurs east of Gifford between the dunbar– 

Gifford Fault and the lammermuir Fault. The formation 

has been proved under younger rocks as far south-west as 

spilmersford. volcanic rocks encountered in a confidential 

borehole at d’Arcy in the midlothian Coalfield are now 

referred to the Garleton Hills volcanic Formation rather than 

an eastward extension of the Arthur’s seat volcanic Formation 

(m A e Browne, verbal communication, 01 march 2007). 

Age 



see also Appendix 1. members of the Garleton Hills 

volcanic Formation in ascending stratigraphical order 

include: 

4.3.14.1 norTH BerwiCK PyroClasTiC MeMBer (nBPy) 

Name 

previously named the North Berwick member (see mcAdam 

and Tulloch, 1985). 

Lithology 

The North Berwick pyroclastic member consists of green 

(lower part in the north) and red (all in the south) tuffs, 

lapilli-tuffs and agglomerate locally with sedimentary 

intercalation of a lacustrine limestone, the sunnyside 

limestone, up to 2.9 m thick. These are commonly well 

bedded and waterlain and interbedded with volcaniclastic 

sedimentary rocks including thin dolostones and siliciclastic 

mudstones with sandstones showing ripple marks. 

Stratotype 

The type area is east lothian [NT 4500 6900 to 6300 8500] 

around North Berwick, east linton, the Garleton Hills, 

and stenton (see davies et al., 1986, fig. 10; mcAdam 

and Tulloch, 1985, fig. 17). Complete reference sections 

are provided by the iGs east linton 2 Borehole (BGs 

Registration Number NT57Ne/2) [NT 59664 77091] from 

about 48.8 to 104.2 m depth, and the spilmersford Borehole 

(BGs Registration Number NT46Ne/73) [NT 4570 6902] 

from about 476 to 544 m depth.


The base is conformable on the underlying Ballagan 

Formation (inverclyde Group). The change is transitional 

by interbedding of tuff and lapilli-tuff into the underlying 

siliciclastic and carbonate rocks. 

The member is overlain by the basaltic lavas of the east 

linton lava member to the south of the dunbar–Gifford 

Fault where the somewhat younger siliciclastic Gullane 

Formation rests directly on it. The contact is conformable 

and locally unconformable. 

Thickness 



east lothian, outcrop of the Garleton Hills volcanic 

Formation around North Berwick, east linton, Garleton 

Hills, stenton and in the subcrop farther west in the BGs 

spilmersford Borehole (see above) near pencaitland, and 

south to the lammermuir Fault. 

Age 

early visean (Chadian to Arundian 

4.3.14.2 easT linTon lava MeMBer (ella) 

Name 

previously named the east linton member (see mcAdam 

and Tulloch, 1985). 

Lithology 

The east linton lava member consists characteristically 

of macroporphyritic basalt and basanite (‘Craiglockhart’ 

type) and hawaiite (‘dunsapie’ type), both with olivine and 

clinopyroxene (large augite) phenocrysts and the latter, also 

with plagioclase. Non-porphyric basaltic trachyandesites 

and a single leucite-bearing analcime trachybasalt (‘kulaite’) 

are also present. Beds of tuff and lapilli-tuff also occur in 

the succession. Flows are usually 5–15 m thick, the upper 

half of each being ‘slaggy’ and vesicular. 

Stratotype 

The type area is east lothian [NT4600 6900 to 6000 8300] 


and stenton (see davies et al., 1986, fig. 10; mcAdam and 

Tulloch, 1985, fig. 17). Reference sections are provided by 

the iGs east linton 2 Borehole (BGs Registration Number 

NT57Ne/2) [NT 59664 77091] which provides a partial 

section through the member from 0 to about 48.8 m depth, 

and the spilmersford Borehole (BGs Registration Number 

NT46Ne/73) [NT 4570 6902], which provides a complete 

section from about 372 to 476 m depth. 


The base is conformable or locally unconformable on the 

North Berwick pyroclastic member. The change is from 

basaltic pyroclastic rocks to basic lavas. 

The member is overlain by the Hailes lava member. 

The contact is conformable and locally unconformable. The 

change is from basalt and basanite and hawaiite to olivine 

basalt and mugearite. 

Thickness 





Hills, stenton and in the subcrop farther west in the BGs 

61 

spilmersford Borehole (see above) near pencaitland, but 

absent adjacent to the lammermuir Fault. 

Age 

early visean (Chadian to Arundian). 

4.3.14.3 Hailes lava MeMBer (Hsla) 

Name 

previously named the Hailes member (see mcAdam and 

Tulloch, 1985). 

Lithology 

The Hailes lava member consists of dark grey, feldsparphyric 

olivine basalts (‘markle’ type) with sparse to abundant, 

large or small feldspar phenocrysts, aphyric basalts and pale 

purple-grey, platy-jointed mugearites. Thicknesses of flows 

are up to 17 m. The feldsar-phyric basalts characterise this 

unit of about six flows. 

Stratotype 



and Hailes (see davies et al., 1986, fig. 10; mcAdam and 

Tulloch, 1985, fig. 17), and in the spilmersford Borehole 

(BGs Registration Number NT46Ne/73) [NT 4570 6902], 

which provides a complete section from about 348 to 372 

m depth. 


The base is conformable or locally unconformable on the 

east linton lava member (olivine-, clinopyroxene- and 

sometimes plagioclase-phyric basaltic lavas; basalt and 

basanite and hawaiite) or locally unconformable on the 

North Berwick pyroclastic member. 

The member is overlain by the Bangley Trachytic 

member. The contact is conformable and locally unconformable. 

The change is from olivine basalt and mugearite 

lavas up into trachytic lavas with trachytic tuff and lapillituff. 

Thickness 





Hills, Hailes and in the subcrop farther west in the BGs 

spilmersford Borehole (see above) near pencaitland, but 

absent south of Hailes adjacent to the dunbar–Gifford 

Fault. 

Age 


4.3.14.4 Bangley TraCHyTiC MeMBer (ByTrC) 

Name 

previously named the Bangley member (see mcAdam and 

Tulloch, 1985). 

Lithology 

The Bangley Trachytic member consists of purple and 

blue-grey trachytic lavas with both feldspar-phyric (sodic 

plagioclase to sanidine) and aphyric types. individual flows 

are known to be over 20 m thick. Quartz-trachytes are also 

present. Red, brown and purple trachytic tuff and lapillituff 

with agglomerate and some volcaniclastic sedimentary 

rocks also are interbedded in units known to be at least 8 

m thick. 



Stratotype 



and stenton (see davies et al., 1986, fig. 10; mcAdam and 

Tulloch, 1985, fig. 17), and in the spilmersford Borehole 

(BGs Registration Number NT46Ne/73) [NT 4570 6902], 

which provides a complete section from about 286 to 

348 m depth. 


The base is apparently conformable on the Hailes lava 

member, which consists of basaltic lavas and volcaniclastic 

rocks. 

The member is overlain by the siliciclastic sedimentary 

rocks of the Gullane Formation (strathclyde Group). The 

contact is considered unconformable with volcaniclastic 

conglomerate recorded locally at the base of the overlying 

formation. 

Thickness 




Formation around North Berwick, east linton, the Garleton 

Hills, and stenton, and in the subcrop farther west in the 

BGs spilmersford Borehole (see above) near pencaitland, 

but absent adjacent to the lammermuir Fault. 

Age 


4.3.15 Gullane Formation (GUL) 

see section 4.3.12 for definition. 

4.3.16 Aberlady Formation (ABY) 

Name 

From Aberlady, east lothian. The formation name was 


Lithology 

The Aberlady Formation consists of a cyclical sequence 

predominantly of pale sandstone interbedded with grey siltstone 

and grey mudstone. subordinate but common lithologies are 

coal, seatrock, ostracod-rich limestone/dolostone and sideritic 

ironstone, and marine bands or bioclastic limestones with 

relatively rich and diverse faunas. The last-named feature 

distinguishes the unit from the Gullane Formation. 


The depositional environment was fluviodeltaic into lakes 

and marine embayments. 

Stratotype 


the spilmersford Borehole (BGs Registration Number 

NT46Ne/73) [NT 4570 6902] (see Browne et al., 1999, fig. 

2, col. 11). other reference sections occur from 28.88 to 

168.10 m depth in the skateraw Borehole (BGs Registration 

Number NT77Nw/47) [NT 7373 7456] and (partially) on 

the coast at Cove [NT 78 71] in the oldhamstocks Basin 

(see Browne et al., 1999, fig. 2, col. 12) and at Kilspindie 

[NT 46 80] by Aberlady Bay. 


The base lies in a transitional sequence and is taken at 

the base of the lowest of the macgregor marine Bands, 



62 

lying above the predominantly sandstone, mudstone and 

siltstone of the Gullane Formation (Figure 6, Column 4e). 

The formation is laterally equivalent to and has a laterally 

transitional boundary with the west lothian oil-shale 

Formation to the west, being distinguished from it chiefly 

by the rarity of oil shales. 

The top of the formation is drawn at the base of 

the Hurlet limestone, located at the base of the lower 

limestone Formation (Clackmannan Group). 

Thickness 


(Chisholm et al., 1989, section 4.4). 


lothians. 


visean (Asbian to Brigantian). mainly Nm miospore Zone 

of Neves et al. (1973) though the vF and TC zones are also 

represented. The macgregor marine bands at the base of 

the formation have a rich and distinctive fauna including 

Punctospirifer scabricosta, Pteronites angustatus and 

Streblopteria redesdalensis, which may be diagnostic. wilson 

(1952) described the B Zone ammonoid Beyrichoceratoides 

redesdalensis from the Cove lower marine Band, the lowest 

of the macgregor marine bands at Cockburnspath. 

4.4 BATHGATE GROUP (BATH) 

The name was first applied by Browne et al. (1999) and 

derives from the town of Bathgate. The sequence comprises: 

At Salsburgh, Lanarkshire, the salsburgh volcanic 

Formation; 

in Fife, the Kinghorn volcanic Formation; 

in West Lothian, the Bathgate Hills volcanic 

Formation. 

These formations are generally characterised by olivine-microphyric 

basalts and basanites of ‘dalmeny’ and 

‘Hillhouse’ types with some olivine-macrophyric basalts of 

‘Craiglockhart’ and ‘dunsapie’ types. Bedded tuffites and 

tuffaceous sedimentary rocks also occur. However, unlike 

the petrologically wide ranging volcanic rocks of the Clyde 

plateau volcanic Formation (strathclyde Group) of the 

western midland valley of scotland, these formations are 

not readily subdivided into members. 

The base of the group is taken at an upward transition 

from sedimentary rocks in most areas, but is drawn at the top 

of the Clyde plateau volcanic Formation in the Rashiehill 


8386 7301], west of slammanan, and at a supposed unconformity 

in the salsburgh 1A oil well (BGs Registration 

Number Ns86sw/89) [Ns 8166 6487]. The top is taken at 

the top of the highest known pyroclastic rock interdigitated 

in the passage Formation (Clackmannan Group) (fluviodeltaic 

(‘Millstone Grit’) facies) in the Central Coalfield area 

(see Cameron et al. 1998, p. 50). 

The type area of the Bathgate Group (not shown on 

Figure 5) is limited in geographical extent to Falkirk, Fife, 

lanarkshire and west lothian, but it interdigitates with a 

large thickness of sedimentary formations, including the 

upper part of the strathclyde Group and the larger part of 

the Clackmannan Group. Asbian to Arnsbergian in age, it 

is very variable in thickness, locally occurring in excess of 

450 m.

4.4.1 Salsburgh Volcanic Formation (Salv) 

Name 

From the type section. The term was first applied by 

Browne et al. (1999). 

Lithology 

The salsburgh volcanic Formation consists of highly 

altered basaltic lavas with sporadic interbeds of limestone, 

mudstone, tuff and tuffaceous mudstone and tuffaceous 

sandstone. 

Stratotype 


the salsburgh 1A oil well (BGs Registration Number 

Ns86sw/89) [Ns 8166 6487] north-west of shotts (see 

Browne et al., 1999, fig. 2, col. 6). 


The early devonian trachytic rocks at the base of the 

salsburgh 1A oil well (see above) have been interpreted 

as intrusive feldspar-macrophyric microgranodiorite 

(or rhyodacite). The contact between the latter and the 

overlying salsburgh volcanic Formation had previously 

been accepted as an unconformity, but now could be 

reinterpreted as intrusive (phillips and Browne, 2000). 

The top of the formation is a conformable transition to 

the cyclical sequence of mainly sandstones with siltstones 

and mudstones of the west lothian oil-shale Formation, 

strathclyde Group. in the type section, a limestone correlated 

with the Burdiehouse limestone rests directly on the 

salsburgh volcanic Formation. 

Thickness 

The maximum known thickness of the formation is 102 m 

in its type section, where the base was apparently not 

reached (phillips and Browne, 2000). 


The formation is only known in its type section (see above). 

Age 

visean (Asbian?) 

4.4.2 Bathgate Hills Volcanic Formation (BHV) 

Name 

From the Bathgate Hills, west lothian. The name was first 

used by smith et al. (1994) to replace earlier terms such as 

‘Bathgate lavas’. it was formally defined by Browne et al. 

(1999). 

Lithology 

The Bathgate Hills volcanic Formation consists of lavas, 

tuffs and volcaniclastic sedimentary rocks. The lavas are 

mostly relatively primitive, silica-undersaturated rocks 

with a restricted range of composition. The ‘basic’ rocks 

are commonly nepheline-normative basanites. The lavas 

are mostly basalt and basanite and olivine-clinopyroxenemicrophyric 

basalt with rare microporphyritic hawaiite. 

weathered ferruginous palaeosols (red boles) are developed. 

The volcanic rocks interdigitate and interact with clastic 

sedimentary rocks of various formations. 


The formation was produced by long-lived series of 

episodes of volcanic activity. The depositional environment 

was mainly terrestrial, at times into water, at times into hot 

springs. 

63 

Stratotype 

The type area comprises natural exposures in the Bathgate 

Hills [Ns 98 75]. A reference section, in which twentysix 

lavas interdigitate with clastic sedimentary rocks, is 

in the Rashiehill Borehole (BGs Registration Number 

Ns87sw/22) [Ns 8386 7301] from 791.6 to 1110.4 m 

depth. 


The base of the formation is taken at the lithological change 

from underlying clastic sedimentary rocks, to lavas, tuffs or 

volcaniclastic sedimentary rocks or at an upward change 

from the petrologically wider range of volcanic rocks 

that form the Clyde plateau volcanic Formation, as in the 

Rashiehill Borehole (see above). in the former case the 

boundary is gradational and is taken where volcanic rocks 

predominate over sedimentary rocks. The top is likewise 

gradational. 

The formation is laterally equivalent to, and interdigitates 

with, the west lothian oil-shale (strathclyde Group), 

and lower limestone, limestone Coal, upper limestone 

and passage formations (Clackmannan Group). 

Thickness 

up to 319 m maximum in the Rashiehill Borehole (see 

above). 


The main outcrop is in the Bathgate Hills, west lothian 

where the rocks crop out in a belt from Bathgate to Bo’ness 

on the coast. The formation has been proved under younger 

rocks as far west as Rashiehill. 

Age 

visean to Namurian (Asbian to Arnsbergian) 

4.4.3 Kinghorn Volcanic Formation (KNV) 

Name 

From the town of Kinghorn, Fife. The term was introduced 

by Browne et al. (1999) to replace earlier informal names 

such as ‘Burntisland lavas’. 

Lithology 

The Kinghorn volcanic Formation consists of basaltic lavas, 

locally with pillows and hyaloclastic textures. volcaniclastic 

sedimentary rocks with subordinate tuffs also occur. The 

lavas are dominantly olivine- and olivine-clinopyroxenephyric 

with rare olivine-clinopyroxene-plagioclase-phyric 

basalts. They are mostly microporphyritic but some 

macroporphyritic varieties also occur. The limited analyses 

available suggest that the lavas are mostly hypersthenenormative. 


The formation is mainly of subaerial origin but locally 

subaqueous. 

Stratotype 

The type section is on the Fife coast between Kinghorn 

and Kirkcaldy [NT 254 863 to 278 882] where about 

460 m of mainly green, olivine-rich, basalt lava can be 

seen in flows interbedded with tuff, sandstone, mudstone 

and marine limestone. The lavas are variably vesicular 

and amygdaloidal, include ophitic textures and pillow 

structures, and may be scoriaceous (see Geikie, 1900, pp. 

53–76; macGregor, 1968, pp. 248–253; Browne et al., 

1999, fig. 2, col. 18). 




The base and top of the formation are usually transitional to 

sedimentary units belonging to the strathclyde Group and 

possibly the basal part of the Clackmannan Group. in the 

type area (see above) the formation is known to interdigitate 

with sedimentary strata of the sandy Craig and pathhead 

formations (Figure 6, Column 4C). 

Thickness 

over 422 m in the seafield No. 1 shaft (BGs Registration 

Number NT28Ne/35) [NT 2769 8953] just south of 

Kirkcaldy. The depth range is from about 134 m to the 

bottom of the hole at about 556 m. The full thickness of the 

formation is therefore not proved. 


Fife. 


visean (Asbian–Brigantian). wilson (1989) favoured 

equation of the 2nd Abden limestone within the type 

section (see above) with the Hurlet limestone at the base of 

the lower limestone Formation, Clackmannan Group and 

also suggested that both Abden limestones may be part of a 

single marine episode that was interrupted by the volcanic 

activity. The associated shales and limestones themselves 

are richly fossiliferous yeilding brachiopods, bivalves, 

gastropods, ostracods, foraminifers, corals and bryozoa. 

The Hurlet limestone is distinguished by the faunal 

sequence (the macnair Fauna) in the underlying mudstone 

(wilson, 1989) and contains typical p 2 ammonoids (Currie, 

1954). 

4.5 CLACKMANNAN GROUP (CKN) 

The term ‘Clackmannan Group’ (Figure 5) was first used in 

the Airdrie district by i H s Hall (BGs, 1992) and Forsyth et 

al. (1996). The succession comprises the lower limestone, 

limestone Coal, upper limestone and passage formations, 

which represent a variable section of mixed shelf carbonate 

and deltaic (‘Yoredale’) facies, fluviodeltaic (‘Millstone 

Grit’) facies and fluviodeltaic (‘Coal Measures’) facies. 

The formations are characterised by strongly cyclical, 

upward-coarsening units of limestone, mudstone, siltstone 

and sandstone capped by coal and seatearth, the proportions 

differing in each of the formations. Thus, beds of laterally 

extensive limestone, with diverse marine faunas, are more 

conspicuous in the lower and upper limestone formations 

than elsewhere; coals are most common in the limestone 

Coal Formation; and sandstones and seatearths (including 

some economically important high-alumina seatclay, fireclay 

and bauxitic clay) are the most prominent constituents of the 

passage Formation. depositional environments, likewise, 

show an underlying similarity, being related to the repeated 

advance and retreat of fluviodeltaic systems into embayments 

of varying salinity. The lower and upper limestone 

formations contain the highest proportion of marine 

deposits (mixed shelf carbonate and deltaic (‘Yoredale’) 

facies), whilst the passage Formation is dominated by 

alluvial deposits (fluviodeltaic (‘Millstone Grit’) facies). 

The limestone Coal Formation occupies an intermediate 

position (fluviodeltaic (‘Coal Measures’) facies). 

The base of the group is taken at the base of the lower 

limestone Formation, where a cyclical sequence of marine 

limestone-bearing strata normally rests conformably on 

various formations of the strathclyde Group. The base of 

the scottish Coal measures Group (fluvio-deltaic (‘Coal 



64 

Measures’) facies) defines the top of the group. 

The type area of the Clackmannan Group is the 

Clackmannan syncline. it extends across the midland 

valley of scotland and includes machrihanish and Arran. 

up to 1800 m thick in the Clackmannan area, the group 

is mostly Namurian in age, but ranges from Brigantian to 

early langsettian. 

The Clackmannan Group also occurs in the southern 

uplands of scotland at sanquhar and Thornhill. in the 

eastern part of the sanquhar Basin the Clackmannan Group 

(undivided) comprises an older, highly variable sequence 

of mainly arenaceous and argillaceous strata, which were 

probably deposited in semi-isolated sub-basins during the 

period of maximum marine transgression. in the west of 

the basin, younger sandstones, siltstones and carbonaceous 

mudstones with marine bands probably represent marginal 

deltaic conditions. The base of the group is unconformable 

on the mainly greywacke sandstones of the ordovician 

Tappins and Barrhill groups, and the top is taken at the 

base of Tait’s marine Band, of possible westphalian age 

(wilson in davies, 1970, p. 52), at the base of the cyclical 

sandstones, siltstones, mudstones, seatrocks and coals of the 

scottish lower Coal measures Formation. in the sanquhar 

Basin the Clackmannan Group is about 40 m thick in total 

and falls within the age range of late visean to langsettian. 

in the Thornhill Basin the Clackmannan Group (see 

section 5.3) comprises the marine–intertidal enterkin 

mudstone Formation of ‘mixed shelf carbonate and deltaic 

(‘Yoredale’) facies’, and the passage Formation of 

‘fluviodeltaic (‘Millstone Grit’) facies’. The base of the 

group is unconformable on the mainly sandstone-dominated 

turbidites of the ordovician Glenlee Formation, leadhills 

supergroup, and the top is taken at the conformable base of 

the scottish lower Coal measures Formation of fluviodeltaic 

(‘Coal Measures’) facies. in the Thornhill Basin the 

Clackmannan Group is up to 55 m thick in total and falls 

within the age range of late visean to pre-westphalian. 

4.5.1 Lower Limestone Formation (LLGS) 

Name 

Forsyth et al. (1996) changed the name lower limestone 

Group to lower limestone Formation, without changes to 

the boundary definitions. 

Lithology 

The lower limestone Formation (see Browne et al., 1999, 

fig. 3) comprises repeated upward-coarsening cycles of 

limestone, mudstone, siltstone and sandstone. The cycles 

may be capped by thin beds of seatearth and coal. The 

limestones, which are almost all marine and fossiliferous, 

are pale to dark grey. The mudstones (many of which also 

contain marine fossils) and siltstones are predominantly 

grey to black. Nodular clayband ironstones and limestones 

are well developed in the mudstones. The sandstones, which 

are usually fine- to medium-grained, are generally offwhite 

to grey. except locally, coal seams are thin (0.3 m) 

and few in number. other minor lithologies include cannel 

and blackband ironstone. A few nonmarine fossiliferous 

beds are known. upward-fining parts of the succession, 

dominated by fine- to medium-grained sandstone but 

lacking limestone, also occur. in the western part of the 

midland valley the sequence is condensed, with the 

intervals between limestones dominated by mudstone. 


The formation comprises mixed shelf carbonate and 

deltaic (‘Yoredale’) facies. The lower parts of the cycles,

including almost all limestones and many mudstones, were 

deposited in marine environments. The upper parts of the 

cycles, including sandstones and coals, were deposited as 

progradational lobate deltas. 

Stratotype 


the wester Gartshore Colliery underground Borehole 


at Kirkintilloch, north-west of Airdrie (see Browne et al., 

1999, fig. 3, col. 4). 


The conformable base of the formation is taken at the base 

of the Hurlet limestone, which is underlain by sedimentary 

rocks of the lawmuir, pathhead, west lothian oil-shale or 

Aberlady formations (Figure 6, Columns 1, 4A–e). 

The top of the formation is drawn at the top of the Top 

Hosie limestone (ToHo), which is overlain by cyclic sedimentary 

rocks of the limestone Coal Formation. 

Thickness 


in the lathallan–Radernie area of east Fife (Forsyth and 

Chisholm, 1977, p. 60). in the western part of the midland 

valley it is condensed to less than 50 m (Browne et al., 

1985). Generalised thickness were given of 45 m on Arran 

(BGs, 1987a) and 8.75 m in the main coalfield area at 

machrihanish (BGs, 1996). 


Throughout the midland valley, the isle of Arran and 

at machrihanish. Browne et al. (1999, table 4) proposed 

a rationalisation of the principal named horizons across 

the midland valley of scotland, using the Glasgow 

nomenclature as the standard. 


visean to Namurian (late Brigantian to early pendleian/early 

serpukhovian). Ammonoids of zonal significance include 

Paradimorphoceras marioni, Metadimorphoceras varians, 

Girtyoceras multicameratum and Beyrichoceratoides 

truncatus var. m all of p 2 age found in the Neilson 

shell Bed, and ‘Cravenoceras’ scoticum of e 1 age found 

below the Top Hosie limestone (Currie, 1954). The 

Hurlet limestone is distinguished by the macrofauna in 

the underlying mudstone. Known as the macnair Fauna, 

its upward sequence includes layers with inarticulate 

brachiopods, bivalves and finally articulate brachiopods 

(see wilson, 1989, p. 104). The mudstones of the Neilson 

shell Bed immediately above the Blackhall limestone 

have a well-preserved fauna including the brachiopod 

Tornquistia youngi (abundant), the gastropods Borestus 

wrighti and Tropidocyclus oldhami and the bivalves 

Euchondria neilsoni, Pernopecten fragilis and Posidonia 

corrugata gigantea, all of which are confined to the 

Neilson shell Bed (wilson, 1989). The faunas of the Hosie 

limestones are rich, though corals are relatively scarce and 

bryozoa are common only in the lower two limestones. 

The bivalve Caneyella membranacea (a very common 

fossil in the higher beds of p 2 age in the pennines area of 

england) is all but confined to the Hosie limestones. it is 

more common in the lower two limestones (wilson, 1989) 

perhaps corroborating Cozar et al. (2008) recognition on 

foraminiferal evidence that the second and Top Hosie 

limestones are both e 1 (pendleian or early serpukhovian) 

in age. Curvirimula is the predominant nonmarine bivalve 

genus in the formation. 

65 

4.5.2 Limestone Coal Formation (LSC) 

Name 

Forsyth et al. (1996) changed the name limestone Coal 

Group to limestone Coal Formation, but without changes 

to the boundaries. 

Lithology 

The limestone Coal Formation (see Browne et al., 1999, 

fig. 4) comprises sandstone, siltstone and mudstone, mostly 

in repeated upward-coarsening cycles, though some fineupwards. 

The cycles are usually capped by seatearth and 

coal. The siltstone and mudstone are usually grey to black, 

while the sandstone is usually fine- to medium-grained and 

off-white to grey. locally named coal seams are common 

and many exceed 0.3 m in thickness. minor lithologies 

include cannel, and blackband and clayband ironstone, the 

latter nodular as well as bedded. Nonmarine limestone is 

rare and marine limestones are present only locally towards 

the bottom of the formation. upward-fining parts of the 

succession, dominated by fine-grained to locally coarsegrained 

sandstone, are widely developed, and thick multistorey 

sandstones are present. locally, successions may 

be particularly sandy or argillaceous. unlike the Johnstone 

shell Bed and ‘Black metals marine Bands’ that can be correlated 

widely, the coal seams are not so easily correlated 

and retain their local names. 


Fluviodeltaic (‘Millstone Grit’) facies. The cycles indicate 

periodic delta progradation, with the ‘marine bands’ 

resulting from marine transgression. 

Stratotype 

Type sections are represented by two boreholes in northeast 

Glasgow; the upper part of the formation from 316.0 

to 539.5 m depth in the Cardowan No. 2 Borehole (BGs 

Registration Number Ns66Ne/66) [Ns 6706 6752] and the 

lower part from 0 to 106.7 m depth in the Cardowan No. 13 

Borehole (BGs Registration Number Ns66Ne/104) [Ns 

6706 6875]. 


The base of the formation is taken at the top of the 

Top Hosie limestone (ToHo) of the lower limestone 

Formation, and the top is drawn at the base of the index 

limestone (ils) of the upper limestone Formation (Figure 

6, Column 4). The lower and upper limestone formations 

include conspicuous beds of laterally extensive limestone, 

with diverse marine faunas, whilst the limestone Coal 

Formation, in contrast, has prominent beds of coal. 

Thickness 

The maximum thickness of the formation is greater than 

550 m in the Clackmannan area of the Central Coalfield 

(Browne et al., 1985, p. 11). in Ayrshire the sequence 

is condensed and less than 100 m thick. Generalised 

thicknesses were given of 110 m for the formation on Arran 

(BGs, 1987a) and 25–105 m in the main coalfield area at 



Throughout the midland valley of scotland, the isle of 

Arran and at machrihanish. 


Namurian (pendleian). Beds containing large numbers of 

shells (coquinas) of Lingula, or of the nonmarine bivalves 



Naiadites and Curvirimula, occur in the fine-grained rocks 

(including ironstones and cannel). Because of the form of 

preservation, these shells usually do not form conspicuous 

‘musselbands’ like those of the scottish Coal measures 

Group. marine shells are present in some fine-grained strata, 

and the Johnstone shell Bed and ‘Black metals marine 

Bands’ can be correlated throughout the midland valley. 

The formation has yeilded no goniatites (Currie, 1954). 

The Johnstone shell Bed is normally developed in two 

beds, the lower carrying the richer faunal assemblage dominated 

by the annelid Serpuloides carbonarius, the brachiopods 

Pleuropugnoides cf. pleurodon, Lingula squamiformis 

and Productus spp., the gastropods Euphemites spp. 

and Retispira spp., and the bivalves Anthraconeilo luciniformis, 

A. mansoni and Streblopteria ornata (wilson, 

1967). The ‘Black metals marine Bands’ yield macrofossils 

including annelids, brachiopods and bivalves (see 

below) in most parts of central scotland, although in some 

areas only Lingula sp. is present. Note that amongst the 

productoid brachiopod genera Productus is dominant in 

the Johnstone shell Bed and rare in the ‘Black metals 

marine Bands’, whilst Buxtonia dominates in the ‘Black 

metals marine Bands’ and is rare in the Johnstone 

shell Bed. Non-marine bivalves are represented in the 

limestone Coal Formation by species of Curvirimula, 

Naiadites and Paracarbonicola. 


see also Appendix 1. members of the limestone Coal 

Formation in stratigraphical order include: 

4.5.2.1 KilBirnie MuDsTone MeMBer (KlMD) 

Name 

The member was previously known as the Kilbirnie 

mudstone Formation. The present definition is that of 

monro (1999; see also Browne et al., 1999; paterson et al., 

1990). 

Lithology 

The Kilbirnie mudstone member comprises mostly dark 

grey mudstone with ironstone, sporadic shelly marine bands 

and siltstone, medium-grained rooted grey sandstone and 

coal. The strata occur in upward-coarsening cycles, some 

capped by thin coal beds. The member includes the dalry 

Clayband ironstone, a grey argillaceous ironstone, and the 

Johnstone shell Bed mudstone, with a marine fauna. 


The cyclical nature of the member indicates periodic delta 

progradation, with the mudstone of the Johnstone shell Bed 

being the result of a marine transgression. 

Stratotype 

The type section is in paduff Burn, starting 200 m north 

of place [Ns 3028 5483] to the centre of Kilbirnie [Ns 

3148 5450] (monro, 1999). Here can be seen some 30 

m of mudstones overlying the Top Hosie limestone. 

They include the dalry Clayband ironstone (0.5 m thick) 

and the Johnstone shell Bed (at least 2.2 m thick) with 

a marine fauna of brachiopods and bivalves. Above this 

bed are upward coarsening sedimentary cycles including 

sandstones (commonly over 4 m thick) and thin coals. 

The sequence is partly intruded by dolerite dykes (monro, 

1999, pp. 50–51). 


The base of the member is taken at the top of the Top 

Hosie limestone (ToHo), the highest of a number of thin 



66 

limestones at the top of the lower limestone Formation 


The top of the member is taken at the lithological change 

from mudstone of the Kilbirnie mudstone member, to the 

overlying dominantly sandstone-bearing cyclical sequences 

of the parent limestone Coal Formation. The upper boundary 

is diachronous. 

Thickness 



North Ayrshire. Not present south of the inchgotrick Fault. 

Age 

pendleian 

4.5.2.2 BlaCK MeTals MeMBer (BKMe) 

Name 

Clough et al. (1916) previously named the member the Black 

metals. it should not to be confused with the locally named 

Black metals (Haughton) marine Band of the Cumberland 

Coalfield which is duckmantian (westphalian B) in age. 

Lithology 

The Black metals member is a thick, laterally persistent dark 

grey mudstone (Read, 1965) distinguished by one or more 

beds, termed ‘Black metals marine Bands’. Read (1965) 

described a sequence within the member of mudstone with 

Lingula at the base; overlain by mudstone with nonmarine 

bivalves or unfossiliferous mudstone, overlain by mudstone 

with a varied marine fauna that comprises the middle part 

of the member; which in turn is overlain by mudstone 

with nonmarine bivalves. The characteristic lithologies of 

the member vary laterally within the midland valley of 

scotland. on the western side of the Central Coalfield in 

the Glasgow district strata that comprise the member are 

described and illustrated by Hall et al. (1998, fig. 11) as 

black and dark grey, carbonaceous mudstones and silty 

mudstones with characteristic development of brownishgrey 

clayband ironstone nodules (California Clayband 

ironstone). sandstones are restricted to thin beds, collectively 

2 or 3 m thick in a total thickness interval of about 32 m. 

eastwards from the Central Coalfield the member includes 

siltstone and sandstone beds that increase progressively in 

number and thickness to become the predominant lithology; 

seatearth and coal also appear (Read, 1965). in the western 

coastal irvine district, the logan’s Bands, comprising 

thin beds of ironstone in a laterally persistent mudstone 

sequence, have been correlated with the Black metals 

member of the Glasgow district (Richey et al., 1930). 


Beds containing shelly marine faunas indicate a marine 

depositional environment (wilson, 1967). However, beds 

with shells including Naiadites sp., indicate nonmarine 

depositional conditions. 

Stratotype 

The type section is north of Glasgow in the Cardowan No. 

2 Bore (BGs Registration Number Ns66Ne/66) [Ns 6706 

6752] from 470 to 502.3 m depth. Reference sections are 

provided in Fife, at the dora opencast Coal site, Area G 

(BGs Registration Number NT19se/550) [NT 1830 9100 

to 1860 9130], and in midlothian, in the monkton House 

Borehole (BGs Registration Number NT37sw/43) [NT 

3325 7044] from about 888 to 907 m depth (see Tulloch 

and walton, 1958, plate 3). Both reference sections include

interbedded sandstone and coal-bearing strata within the 

member. 


in the Central Coalfield the base of the mudstone comprising 

the member is picked at the top of the Black metals Basal 

Coal (Forsyth and Read, 1962). eastwards the base is 

picked at the top of a laterally equivalent seatearth and 

correlated to a thin coal above the Torrance Four-inch Coal 

farther east in Fife (Read, 1965, fig. 2). westwards, in the 

Glasgow district, marine fossils are recorded just above 

the base of the Black metals member, the boundary being 

picked at the roof of the upper Garscadden Coal which 

here may be developed as a blackband ironstone (upper 

Garscadden ironstone) (Hall et al., 1998, fig. 11; Forsyth 

and Read, 1962). 

At its upper boundary in the Central Coalfield, mudstone 

of the Black metals member is interbedded with sandstone 

of the overlying limestone Coal Formation (Figure 6, 

Column 4). The boundary is picked at the base of the lowermost 

bed of coarse siltstone or sandstone (Read, 1965). 

in the Bo’ness area of the livingson district (Read, 1965), 

the erosive base of the sandstone has cut down into the 

member, or it is abruptly overlain by lavas of the Bathgate 

Hills volcanic Formation. in the Glasgow district the upper 

boundary of the Black metals member is just below (within 

about 5 m of) the Knott Coal horizon (Hall et al., 1998, 

fig. 11). 

Thickness 

Read (1965) described the thickness of the member as 

exceeding that of typical fining-upwards cycles of the 

limestone Coal Formation, which are usually about 3–10 m 

thick. North of Glasgow on the western side of the Central 

Coalfield in the Cardowan No. 2 Bore (see above) the 

member is 32.3 m thick (from 470 to 502.3 m depth) (Hall et 

al., 1998, fig. 11). The thickness is similar in the Kincardine 

and Fife–midlothian basins. However, in the Kincardine 

Basin in west Fife the thickness of the member increases 

eastwards from 33 m to a maximum of 66 m, associated 

with the lateral change to an increasingly sandstone-bearing 

succession (Francis et al., 1970, p. 190, and plate 8). 


Central scotland, but not identified in southern and central 

Ayrshire by simpson and macGregor (1932) or eyles et al. 

(1949). 


pendleian. The ‘Black metals marine Bands’ yield 

macrofossils in most parts of central scotland although 

in some areas only Lingula is present. The annelid 

Serpuloides carbonarius, the brachiopods Buxtonia spp., 

Pleuropugnoides cf. pleurodon and Lingula spp. and the 

bivalve Streblopteria ornata are the main forms. The 

bivalve Aviculopinna mutica is commonly present in 

midlothian and Fife, but has not been found elsewhere 

(wilson, 1967). The member also includes beds with a 

nonmarine shelly fauna including Naiadites sp. The logans 

Bands in the western coastal irvine district contain Lingula 

and Naiadites or nonmarine bivalves (monro, 1999). 

4.5.3 Upper Limestone Formation (ULGS) 

Name 

Forsyth et al. (1996) changed the name upper limestone 

Group to upper limestone Formation. The boundary 

definitions were unaffected. 

67 

Lithology 

The upper limestone Formation (see Browne et al., 1999, 

fig. 5) is characterised by repeated upward-coarsening 

cycles comprising grey limestone overlain by grey to black 

mudstones and calcareous mudstones, siltstones and paler 

sandstones capped by seatrocks and coal. The limestones 

contain marine faunas and are usually argillaceous. These 

limestones are laterally extensive and have standard 

names that can be used throughout the midland valley. 

The proportion of limestone increases to the west. The 

sandstones are generally off-white and fine- to mediumgrained. 

The coals are usually less than 0.6 m thick. minor 

lithologies include ironstone and cannel, and there are some 

volcanic rocks. upward-fining sequences of coarse- to finegrained 

sandstones passing up into finer-grained rocks are 

also present. 


The formation comprises mixed shelf carbonate and 

deltaic (‘Yoredale’) facies. The lower parts of the cycles, 

including almost all limestones and many mudstones, were 

deposited in marine environments. The upper parts of the 

cycles, including sandstones and coals, were deposited as 

progradational lobate deltas. The increase in the proportion 

of limestone to the west, indicates increasingly marine 

conditions in that direction (Francis, 1991). 

Stratotype 

The type section of the upper limestone Formation is the 

mossneuk Borehole (BGs Registration Number Ns88Ne/204) 

[Ns 8723 8609], south of Alloa, between 335.0 and 770.3 m 

depth (see Browne et al., 1999, fig. 5, col. 6). 


The base of the formation is taken at the base of the index 

limestone (ils) or, locally, at a plane of disconformity, 

in both cases underlain by cyclic sedimentary rocks of the 

limestone Coal Formation (Figure 6, Column 4). 

where the upper limestone Formation is fully developed, 

the top is drawn at the top of the Castlecary limestone 

(CAs), overlain by cyclic sedimentary rocks of the passage 

Formation. 

Thickness 

The maximum thickness of the formation is over 600 m in 

the Clackmannan area of the Central Coalfield (Browne 

et al., 1985, p. 11). it is less than 100 m thick in Ayrshire. 

Generalised thickness were given of 90–140 m on Arran 

(BGs, 1987a) and 87.5 m in the main coalfield area at 



Throughout the midland valley of scotland, the isle of 

Arran and at machrihanish. 


Namurian (pendleian to Arnsbergian). Ammonoids 

including Tumulites pseudobilinguis recovered from 

the index limestone, Eumorphoceras bisulcatum 

grassingtonense from the orchard limestone, E. B. 

ferrimontanum and ‘Cravenoceras’ gairense from the 

Calmy limestone, and Cravenoceratoides nitidus from 

the Castlecary limestone provide evidence for the e 1b 2 

to e 2b 2 age of the formation (see Ramsbottom, 1977b). 

According to wilson (1967) the brachiopod Antiquatonia 

costata is only found in the orchard limestone, whilst 

Pugnax cf. pugnus and Sinuatella cf. sinuata (with the 

bivalve Actinopteria regularis) are only associated with the 



Calmy limestone. The gastropods Meekospira sp. in the 

index limestone, Straparollus (Euomphallus) carbonarius 

in the orchard limestone and Euphemites ardenensis with 

the bivalve Edmondia punctatella in the Calmy limestone 

fauna have short vertical ranges with their acme at the level 

mentioned. The bivalve Streblopteria ornata disappears 

after ranging up to the lyoncross limestone, whilst the 

nautiloid Tylonautilus nodiferus has not been found below 

the Calmy limestone. The nonmarine bivalve genera in the 

formation are Curvirimula and Naiadites. 

4.5.4 Passage Formation (PGP) 

Name 

Forsyth et al. (1996) changed the name passage Group 

to passage Formation. The boundary definitions were 

unaffected. 

Lithology 

The passage Formation (see Browne et al., 1999, fig. 6) is 

characterised by an alternation of fine- to coarse-grained 

sandstones (with some conglomerates) and structureless 

clayrocks (including some high-alumina seatclay, fireclay 

and bauxitic clay). The clayrocks are commonly mottled 

reddish brown and greenish grey. upward-fining cycles 

predominate over upward-coarsening cycles. Bedded grey 

and black siltstones and mudstones are also present, and 

beds of limestone, ironstone, cannel and coal. marine 

faunas, diverse and closely spaced at the base, become 

progressively impoverished upwards. volcanic rocks also 

occur. 


Fuviodeltaic (‘millstone Grit’) facies. 

Stratotype 

The type section of the passage Formation occurs between 

48.95 and 368.15 m depth in the saltgreen No. 1 Borehole 

(BGs Registration Number Ns98Nw/197) [Ns 9196 

8608], south of Clackmannan (see Browne et al., 1999, 

fig. 6, col. 6). 


The base is taken at the top of the Castlecary limestone 

(CAs) or at a plane of disconformity where the base is 

erosive, both underlain by cyclic sedimentary rocks of the 

upper limestone Formation (Figure 6, Column 4). The 

top is drawn at the base of the lowstone marine Band 

(lomB) or a correlative, marking the base of the scottish 

Coal measures Group. it has been suggested (see Read, 

1981, Read et al., 2002, pp. 281–282) that, in the area 

of greatest thickness, the formation includes up to three 

major disconformities. These apparently cut out strata of 

mid Arnsbergian, late Arnsbergian to late Alportian, and 

Kinderscoutian to marsdenian age and may include the mid 

Carboniferous break. in some areas, such as douglas, two 

unconformities have been proved. 

The passage Formation also occurs in the Thornhill 

Basin, where the sandstone facies (including grey, white 

and pink pebbly sandstone with beds of conglomerate) 

lie conformably or disconformably on the carbonate 

and siliciclastic rocks of the late Asbian to Brigantian 

Closeburn limestone Formation (yoredale Group) (Figure 

6, Column 6), or unconformably on the mainly sandstone 

turbidites of the ordovician Glenlee Formation or silurian 

Gala Group. They are overlain by the fluviodeltaic (‘Coal 

Measures’) facies of the scottish lower Coal measures 

Formation. 



68 

Thickness 


in the Clackmannan area of the Central Coalfield (Browne 

et al., 1985, p. 10). Generalised thicknesses were given of 

0–50 m on Arran (BGs, 1987a) and 152.5 m in the main 

coalfield area at machrihanish (BGs, 1996). 


Throughout the midland valley of scotland, on the isle of 

Arran, at machrihanish, and in the Thornhill Basin and the 

western part of the sanquhar Basin. 


Namurian to westphalian (Arnsbergian to langsettian), 

lower so to lower ss miospore zones. Ammonoids 

are rare. Anthracoceras glabrum and A. paucilobum of 

Arnsbergian (e 2 ) age have been recovered from shortly 

above the Castlecary limestone (see Currie, 1954), and 

Homoceratoides sp. of apparently Kinderscoutian (R 1 ) age 

has been found probably within the No.3 marine Band 

group (Neves et al., 1965). Neves et al. (1965) located 

spore assemblages of lower Kinderscoutian (R 1 ), uppermost 

marsdenian (R 2 ), by implication yeadonian (G 1 ), and 

lower langsettian (G 2 ) age in the scottish Namurian and 

westphalian, but found no evidence of the Chokierian 

(H 1 ) or Alportian (H 2 ) stages. The No.2 marine Band, 

which is developed in places as a thin, impure limestone 

(the Roman Cement limestone) is largely composed of 

crushed brachiopod valves. The mudstone and ironstone 

marine bands in the formation have dominantly brachiopods 

including orthotetoids, Productus cf. carbonarius and 

Schizophoria cf. resupinata and the bivalve Schizodus taiti 

(wilson, 1967). The nonmarine bivalve genus Curvirimula 

is abundant in the immediate roof mudstone of the Castlecary 

limestone, which forms the uppermost bed of the upper 

limestone Formation (see above). 


see also Appendix 1. members of the passage Formation in 

ascending stratigraphical order include: 

4.5.4.1 Troon volCaniC MeMBer (Tvl) 

Name 

Named after the town of Troon and previously known as the 

‘Troon volcanic Formation’ and ‘passage Group lavas’. 

The present member was defined by monro (1999); see also 

Browne et al. (1999). 

Lithology 

The Troon volcanic member comprises olivine-microphyric 

basalt (‘dalmeny’ type). 

Stratotype 

Type sections occur in the lugton water [Ns 332 447] 

where a full sequence through the lavas is exposed, but the 

total thickness is only about 10 m and the lavas are highly 

decomposed. Additionally, the member was encountered in 

the BGs Gailes Farm Borehole (BGs Registration Number 

Ns33sw/1) [Ns 32788 34867] from about 32.84 to 207.68 

m depth. 


The lower boundary of the member is taken at the lithological 

change from sandy clastic strata of the underlying parent 

passage Formation to basaltic lava. 

The upper boundary of the member is taken at the base 

of the Ayrshire Bauxitic Clay member and is defined as 

the lithological change from olivine-microphyric basalt

to bauxitic clay. This boundary is described as normally 

gradational. 

Thickness 

some 10 m thick at lugton water and about 175 m in the 

BGs Gailes Farm Borehole (see above). 


North and central Ayrshire 

Age 

Namurian 

4.5.4.2 ayrsHire BauxiTiC Clay MeMBer (aBC) 

Name 

Formerly known as the Ayrshire Bauxitic Clay Formation 

(monro, 1982). see also monro (1999); Browne et al. 

(1999). 

Lithology 

pale grey to buff clayrock, of massive habit with conchoidal 

fracture, hard and compact. Texture ranges from fine-grained 

to oolitic, pisolitic and coarsely clastic. mineralogically, 

‘bauxitic in the chemical sense of containing more Al 2 o 3 

than can be accommodated with sio 2 to give kaolinite’. The 

bauxitic clay may be considered a flint clay. The member 

may also contain sphaerosiderite, fossil plant fragments and 

tree trunks and include beds of seatrock, coal and mudstone. 

Stratotype 

The type section is the saltcoats shore [Ns 2401 4150]. 

Here the section into the bauxitic clay is about 1.2–1.5 m 

thick and consists of a massive, pale grey, to buff clayrock 

with steep joints. dark grey plant scraps are common 

and ooliths and pisoliths are present. sphaerosiderite is 

common and varies in abundance through the bed. There 

is a gradational passage into an underlying clayrock, which 

further grades into basaltic lavas of the Troon volcanic 

member (monro, 1999, p. 65). 


The base is taken at the lithological change from olivinemicrophyric 

basalt of the underlying Troon volcanic 

member and is gradational from basalt through clayrock rich 

in sphaerosiderite to bauxitic clay. The base is considered to 

be stratiform, although it may be obscured by later lateritic 

weathering or diagenesis and some in-situ alteration of 

basalt to bauxitic clay may have occurred. 

The top of the member is taken at the base of the scottish 

lower Coal measures. in Ayrshire this is marked by the 

Raise Coal seam that lies immediately above the Ayrshire 

Bauxitic Clay. 

Thickness 

up to about 20 m 


limited to north Ayrshire and parts of central Ayrshire. 

Age 

Namurian to westphalian (langsettian) 

4.6 SCOTTISH COAL MEASURES GROUP 

(CMSC) 

The ‘Coal measures’ were regarded as a lithostratigraphical 

group by Forsyth et al. (1996). The epithet ‘scottish’ was 

69 

proposed by waters et al. (2007) to distinguish the ‘Coal 

measures’ of scotland from those of england and wales to 

account for the different definitions of the base of the upper 

Coal measures and the base of the groups. 

The scottish Coal measures Group (Figure 5; Browne 

et al., 1999, fig. 7) (fluviodeltaic (‘Coal Measures’) 

facies) is divided, in ascending sequence, into scottish 

lower, middle and upper Coal measures formations. 

lithologically the group comprises repeated cycles of 

sandstone and mudstone with coal and seatearth, arranged 

in both upward-fining and upward-coarsening units. The 

strata are generally grey in colour but are extensively 

reddened towards the top. A wide range of alluvial and 

lacustrine environments of deposition is represented. 

These include wetland forest and soils (coal and seatrock), 

floodplain (planty or rooted siltstone and mudstone), river 

and delta distributary channel (thick sandstones), prograding 

deltas (upward-coarsening sequences) and shallow 

lakes (mudstones with nonmarine faunas). marine bands 

are rare but provide important stratigraphical markers. 

economically important coal seams are common in the 

lower and middle Coal measures, some of which can be 

correlated between coalfields. 

The base of the group in the midland valley of scotland 

is now taken at the base of the lowstone marine Band, its 

local correlative, or at a plane of disconformity. This is at 

a slightly higher stratigraphical level than in england and 

wales, where the lower boundary lies at the base of the 

subcrenatum marine Band at the base of the langsettian 

(westphalian A) stage. This horizon has not been recognised 

in scotland though it may correlate with one of the 

higher marine bands of the passage Formation (No. 6) and 

with the porteous marine Band of the douglas Coalfield. 

An unconformity of regional extent beneath permian strata 

marks the top of the scottish Coal measures Group in the 

midland valley of scotland. 

The scottish Coal measures Group occurs in the midland 

valley of scotland and adjacent areas including sanquhar, 

Thornhill, machrihanish, Arran, stranraer and morvern. 

probably exceeding 1790 m in the midland valley of 

scotland, it is langsettian to Asturian (westphalian d) in 

age. it is considered that no stephanian rocks have been 

identified in the midland valley of scotland. However, see 

wagner (1983), details provided below. 

4.6.1 Scottish Lower Coal Measures Formation (LCMS) 

Name 

The epithet ‘scottish’ is applied to the lower Coal measures 

to distinguish them from the formation in england and 

wales on account of the different definition of the base of 

the formation (and group) (waters et al., 2007). 

Lithology 

The scottish lower Coal measures comprise sandstone, 

siltstone and mudstone in repeated cycles, which most 

commonly coarsen-upwards, but also fine-upwards, with 

seatearth and coal at the top. The mudstones and siltstones 

are usually grey to black, while the sandstone is fine- to 

medium-grained and off-white to grey. Coal seams are 

common and many exceed 0.3 m in thickness. minor 

lithologies include cannel and blackband and clayband 

ironstone, the latter nodular as well as bedded. Bands 

composed mainly of nonmarine bivalves, the characteristic 

‘musselbands’, usually occur in mudstone or ironstone. 

upward-fining parts of the succession, dominated by fine- 

to coarse-grained sandstone, are widely developed and thick 

multistorey sandstones are a feature. 




Fluviodeltaic (‘Coal Measures) facies. The depositional 

environments include prograding deltas (upwardcoarsening 

sequences), floodplain (planty or rooted 

siltstone and mudstone), shallow lakes (mudstones with 

nonmarine faunas), river and delta distributary channel 

(thick sandstones) and wetland forest and soils (coal and 

seatrock). marine bands will have resulted from marine 

transgressions. 

Stratotype 

The type section of the formation is between 187.50 and 

301.19 m depth in the Clyde Bridge, motherwell Borehole 

(BGs Registration Number Ns75Nw/68) [Ns 7380 5622] 

in the west Central Coalfield (see Browne et al., 1999, 

fig. 7, col. 4). 


The base of the scottish lower Coal measures is taken at 

the base of the lowstone marine Band (lomB), its local 

correlative, or at a plane of disconformity. it is underlain by 

cyclical sedimentary rocks of the passage Formation (Figure 

6, Column 4). This is at a slightly higher stratigraphical 

level than in england and wales (see section 4.6 above). 

The top of the formation lies at the base of the 

vanderbeckei (Queenslie) marine Band (vdmB), or its 

local equivalent, at the base of the scottish middle Coal 

measures. 

Thickness 

The maximum thickness of the formation is between 

220 and 240 m in the sealab No. 2 Borehole (BGs 

Registration Number NT38sw/1) [NT 3272 8449] in 

the Firth of Forth from about 220 to 500 m depth. The 

variation in thickness is a function of correction for 

stratal dip (see Browne et al., 1999, p. 18). Generalised 

thickness were given of about 65 m on Arran (BGs, 

1987a) and 67.5 m in the main coalfield area at 



The midland valley of scotland, on the isle of Arran, 

at machrihanish, and in the small basins of the southern 

uplands (excluding solway). 


westphalian A (langsettian). ss to RA miospore zones 

of Clayton et al. (1977). The most abundant fauna of 

the formation is the nonmarine bivalves of the upper 

lenisulcata, Communis and lower modiolaris chronozones 

(see Trueman and weir, 1946; Calver, 1969). Genus 

Carbonicola dominates and includes, for example, in 

the upper lenisulcata Chronozone C. extenuata, in the 

Communis Chronozone C. polmontensis, C. pseudorobusta 

and C. oslansis, and in the lower modiolaris Chronozone 

C. venusta (see Cameron and stephenson, 1985, fig. 29). 

The lowstone marine Band at the base of the formation is 

commonly developed as a Lingula band as too is the small 

group of up to three marine bands present near the top of the 

lenisulcata Chronozone. 

4.6.2 Scottish Middle Coal Measures Formation 

(MCMS) 

Name 

The epithet ‘scottish’ is applied to the middle Coal 

measures to distinguish them from the formation in england 

and wales (waters et al., 2007). 



70 

Lithology 

The scottish middle Coal measures comprise similar 

lithologies to the scottish lower Coal measures (see 

section 4.6.1 above). 


Fluviodeltaic (‘Coal Measures’) facies. The depositional 

environments include prograding deltas (upward-coarsening 

sequences), floodplain (planty or rooted siltstone and 

mudstone), shallow lakes (mudstones with non-marine 

faunas), river and delta distributary channel (thick 

sandstones) and wetland forest and soils (coal and seatrock). 

marine bands resulted from marine transgressions. 

Stratotype 

The type section of the upper part of the scottish middle 

Coal measures (from the base of ‘skipsey’s marine 

Band’ marking the top of the formation, to the drumpark 

marine Band) is from 9.5 to 26.0 m depth in the dalzell 

works, motherwell Bore No. 4 (BGs Registration 

Number Ns75Ne/316) [Ns 7571 5672]. For the lower 

part of the formation (from the drumpark marine Band 

to the ‘Queenslie marine Band’ at the base) the type 

section is from 18.29 to 187.50 m depth in the Clyde 

Bridge, motherwell Borehole (BGs Registration Number 

Ns75Nw/68) [Ns 7380 5622]. A section containing a 

full development of the vanderbeckei (Queenslie) marine 

Band (vdmB) is present from 15.24 to 37.49 m depth in 

the moffat mills water Bore (BGs Registration Number 

Ns76se/77A) [Ns 7898 6499] east of Airdrie. All three 

of these sections are in the west Central Coalfield (see 

Browne et al., 1999, fig. 7, col. 4). 


The base of the scottish middle Coal measures is taken 

at the base of the vanderbeckei (Queenslie) marine 

Band (vdmB) or its local equivalent, overlying cyclical 

sedimentary rocks of the scottish lower Coal measures 

(Figure 6, Column 4). where this horizon cannot be 

established, the closest approximation based on nonmarine 

bivalve faunas is taken. in North Ayrshire this is the top of 

the shale Coal. 

The top of the scottish middle Coal measures is drawn 

at the base of the Aegiranum (skipsey’s) marine Band 

(AGmB), forming the base of the scottish upper Coal 

measures. 

Thickness 


based on the dip corrected section of the sealab No. 1A 

Borehole (BGs Registration Number NT38Nw/31) [NT 

3230 8568] in the Firth of Forth from about 32 to 340 

m depth, and exposures on the Fife Coast between west 

wemyss [NT 321 947] and Buckhaven [NT 351 976]. 

Generalised thicknesses were given of about 50 m on 

Arran (BGs, 1987a) and 95 m in the main coalfield area at 



The midland valley of scotland, on the isle of Arran, 

at machrihanish, and in the small basins of the southern 

uplands (excluding the solway). 


westphalian B (duckmantian). NJ miospore Zone of 

Clayton et al. (1977). The most abundant fauna of 

the formation is the non-marine bivalves of the upper 

modiolaris and lower similis-pulchra chronozones

(see Trueman and weir, 1946; Calver, 1969). Genus 

Anthracosia dominates and includes, for example, 

in the upper modiolaris Chronozone A. ovum and A. 

phrygiana, and in the lower similis-pulchra Chronozone 

A. caledonica and A. atra (see Cameron and stephenson, 

1985, fig. 29). The vanderbeckei marine Band at the base 

of the formation attains ‘goniatite-pectenoid’, ‘productoid’ 

and Lingula facies. its varied fauna may include in 

places the ammonoid Anthracoceras sp. with the bivalve 

Dunbarella sp., brachiopods (including productoids), 

or just Lingula (see Calver, 1969). A group of up to 

four marine bands occurs in the lower similis-pulchra 

Chronozone, usually only with Lingula, but with bivalves 

present in a few areas. 

4.6.3 Scottish Upper Coal Measures Formation (UCMS) 

Name 

The epithet ‘scottish’ is applied to the upper Coal measures 

to distinguish them from the formation in england and 

wales on account of the different definition of the base of 

the formation (waters et al., 2007). 

Lithology 

The scottish upper Coal measures comprise sandstone, 

siltstone and mudstone in repeated cycles, which most 

commonly fine-upwards. The mudstone occurs most 

commonly as structureless beds and seatearth. The sequences 

are usually reddish brown and purplish grey. Coal seams are 

not common, are normally less than 0.3 m thick and may be 

replaced, totally or in part, by red (haemetitic) and dark grey 

carbonaceous diagenetic limestone. Brecciation textures 

may occur and nodular pedogenic carbonate is present in 

some clay/silt grade rocks in Fife. 


Fluviodeltaic (‘Coal Measures) facies. The reddish brown 

and purplish grey colours are due to oxidation of originally 

grey strata beneath the permian unconformity, but some 

reddening may be primary, related to periods of lowered 

water table during deposition. 

Stratotype 

The partial type section of the scottish upper Coal measures 

is from surface to 285 m depth in the Hallside Borehole 

(BGs Registration Number Ns65Ne/66) [Ns 6693 5974] 

south-east of Glasgow in the west Central Coalfield (see 

Browne et al., 1999, fig. 7, col. 4). Reference sections are 

provided by the Killoch No. 1 Bore (BGs Registration 

Number Ns42se/7) [Ns 4756 2023] from the sub-permian 

unconformity at 39.9 m depth to an ‘ashy conglomerate’ 

at 123.6 m depth (the strata at 63.9 m depth including 

Anthraconaia pruvosti of the undifferentiated phillipsii 

and Tenuis chronozones), and the Killoch No. 1A Bore 


which continues the section from 123.6 m depth at the 

‘ashy conglomerate’ mentioned above, to the Aegiranum 

(skipsey’s) marine Band at 481.3 depth. 


The base of the formation is drawn at the base of the 

Aegiranum (skipsey’s) marine Band (AGmB) (Forsyth 

et al., 1996; Browne et al., 1999, p.19), which is underlain 

71 

by cyclical sedimentary rocks of the scottish middle Coal 

measures (Figure 6, Column 4). in Fife and lothian this 

bed has been tentatively recorrelated with the ‘Buckhaven 

Planolites Band’ and the montague Bridge marine Band 

(see Browne et al., 1999, and references therein). The 

Aegiranum marine Band is at a lower stratigraphical level 

than the Cambriense marine Band, the top of which marks 

the base of the pennine upper Coal measures. 

The top of the scottish upper Coal measures is marked 

by an erosional unconformity of regional extent beneath 

permian strata. 

Thickness 

Based on the interpretation of commercial seismic data 

the maximum thickness of the formation probably exceeds 

1200 m under the Firth of Forth. up to 460 m in central 

Ayrshire. A generalised thickness of 280 m in the main 

coalfield area at machrihanish was given by BGs (1996). 


The midland valley of scotland, machrihanish and the 

small basins of the southern uplands (excluding solway). 


westphalian C–d (Bolsovian–Asturian). The fauna of 

the formation includes, in its lower parts, nonmarine 

bivalves of the upper similis-pulchra and the combined 

phillipsii and Tenuis chronozones. Anthraconaia adamsi, 

A. spathulata and Naiadites hindi may, for example, occur 

in the upper similis-pulchra Chronozone, and A. pruvosti, 

Anthraconauta phillipsii and An. tenuis in phillipsii/ 

Tenuis strata (see Trueman and weir, 1946; mykura, 1967; 

Calver, 1969; Cameron and stephenson, 1985, fig. 29). 

The Aegiranum marine Band at the base of the formation 

has a rich and varied ‘benthonic and cephalopod’ fauna 

with calcareous brachiopods, ammonoids and nautiloids 

(see Calver, 1969). There is no evidence of marine 

conditions above the upper similis-pulcra Chronozone. 

in the upper part of the upper Coal measures only scarce 

plant remains and the annelid Spirorbis sp. are found 

(Cameron and stephenson, 1985). Floras indicative of the 

Bolsovian and Asturian stages have been identified (scott, 

1976). 

plant impressions from a sedimentary intercalation in the 

mauchline volcanic Formation exposed in the River Ayr 

near stairhill [Ns 4521 2423] were formerly regarded as 

being characteristic of an Asturian (westphalian d) or more 

likely late stephanian age (see wagner, 1966; mykura, 

1967, pp. 25, 27, 80; Ramsbottom et al., 1978, fig. 14:4, 

p. 62). However, with further evidence, including the presence 

of Lobatopteris geinitzii (von Gutbier, emend. sterzel) 

comb. nov., wagner (1983; see also Brand, 1983, p. 175 

and references therein) was able to compare the assemblage 

with lower Rotliegend floras of central europe and give it 

a probable early permian (early Autunian; Asselian) age, 

which is still accepted (see Cleal and Thomas, 1995, pp. 

229–233). However, biostratigraphical problems associated 

with geologically long-lived plant genera, phylogenic variation, 

climate change and the potential of mixed diachronous 

and refugial floral assemblages at the Carboniferous– 

permian boundary make desirable an independent reinterpretation 

of the fossil flora and palynology at the stairhill 

site (Hilton in dean, 2002). 



5 Carboniferous rocks of the southern uplands of scotland 

5.1 THE SANQUHAR AND THORNHILL BASINS 

The sanquhar and Thornhill basins (Figure 6, Columns 5, 6) 

occupy much of the valley of the River Nith. At sanquhar 

the beds mostly belong to the scottish Coal measures 

(the scottish lower, middle and upper Coal measures 

formations all being present), but small thicknesses of the 

Clackmannan Group (undivided) and the passage Formation 

are present below an unconformity. At Thornhill, rocks of 

the yoredale Group (Closeburn limestone Formation), 

Clackmannan Group (enterkin mudstone and passage formations) 

and scottish Coal measures Group (including the 

scottish lower, middle and upper Coal measures formations) 

are recognised. 

5.2 YOREDALE GROUP (YORE) 

The yoredale Group, as defined in full in section 6.7, is 

restricted to the Thornhill Basin, with a single formation, 

the Closeburn limestone Formation. 

5.2.1 Closeburn Limestone Formation (CLO) 

Name 

From Closeburn, south of Thornhill, dumfries and 

Galloway. defined as a formation by mcmillan (2002; 

see also menteath, 1845; pringle and Richey, 1931; Jones, 

1994). 

Lithology 

The formation consists dominantly of limestone and 

dolomitic limestone with interbedded sandstone, siltstone 

and mudstone. 


The fauna (see below) of the limestone indicates that it is 

marine. 

Stratotype 

A partial type section occurs in upper Closeburn Quarry 

(Croalchapel Quarry) [NX 9100 9170 to 9120 9130]. This 

section is in the upper part of the formation lying above 

the upper of two limestones separated by 5.5 m of strata. 

These limestone beds were noted by Geikie (1877) but 

are not visible today. pringle and Richey (1931) indicated 

that about 12 m of sandstone, shale and fireclay lie above 

the upper limestone. mcmillan (1991, and references 

therein) provided logs of sections recorded in Croalchapel 

Quarry in 1962 at [NX 9109 9159] with siltstone (2.4 m), 

limestone (0.5 m) and sandstone (7.2 m) and at [NX 

9109 9150] with siltstone (0.7 m), mudstone (0.1 m) 

and sandstone (1.8 m). A good section in the Closeburn 

limestone Formation was cored in the BGs Closeburn 

Borehole (BGs Registration Number NX99sw/2) [NX 

9021 9145] between about 6.5 and 29.7 m depth, but the 

presence of unconformities at both the top and bottom of 

this section suggest the full thickness of the formation is 

not represented. 



72 


The unconformable base of the formation is taken where the 

greywacke sandstone of the underlying silurian Gala Group 

passes upward into dominantly limestone strata. 

The top of the formation is apparently conformable or 

disconformable with the base of the overlying grey, white 

and pink pebbly sandstone with beds of conglomerate of the 

passage Formation (Figure 6, Column 6). 

Thickness 

The maximum thickness of the formation is about 25 m. 


The formation is limited to the Thornhill Basin. The fauna 

of the limestones suggests correlation with strata in the 

upper part of the Tyne limestone Formation or Alston 

Formation (yoredale Group) of the solway Basin. 


late visean (late Asbian to Brigantian). The formation 

has corals, brachiopods (incuding productoids, 

gigantoproductoids and orthotetoids), gastropods, bivalves 

(including nuculids and various species of Edmondia and 

Leiopteria), orthocone and coiled nautiloids (including 

large specimens of the former) and fish. The overall aspect 

of the fauna suggests a late visean (late Asbian, B 2 to 

Brigantian, p 2 ) age (see mcmillan, 2002; Table 2). 

5.3 CLACKMANNAN GROUP (CKN) 

The Clackmannan Group, as defined in full in section 4.5, 

is present in both the sanquhar and Thornhill basins. 

SANQUHAR BASIN 

in the sanquhar Basin the Clackmannan Group has not been 

formally divided into constituent formations. However, 

lower and upper sequences within the group are recognised. 

5.3.1 Clackmannan Group (CKN) (undivided) 

Name 

see section 4.5 for definition. details relevant to the 

sanquhar Basin are provided below: 

Lithology 

The lower sequence, formerly called the ‘Carboniferous 

limestone series’, comprises basal conglomerate or breccia 

that passes up into sandstone, which in turn is overlain by 

fossiliferous, grey, calcareous mudstone and siltstone with 

local impure limestone beds and thin coals and seatclays. 

The unit shows marked lateral variations in lithology. The 

upper sequence, formerly called the ‘millstone Grit series’, 

comprises coarse-grained, greenish sandstone at the base, 

superseded by greyish-white, cross-bedded sandstones, 

grey, brown and purple siltstones, and carbonaceous 

mudstones with marine bands overlain by kaolinitic beds. 

The unit shows lateral variations in lithology, and local 

unconformities are present.


The marked lateral variations in lithology in the lower 

sequence, suggest deposition probably occurred in semiisolated 

sub-basins during the period of maximum marine 

transgression. The lateral variations in lithology and the 

presence of local unconformities and marine bands in the 

upper unit, suggest local deposition of condensed sequences 

in marginal deltaic conditions. 

Stratotype 

Reference sections are exposed for the lower sequence 

in Howat’s Burn [Ns 828 097] near sanquhar with 

conglomerate, sandstone, calcareous mudstone and shelly 

fossiliferous limestone, and for the upper sequence in 

Barr Burn [Ns 759 089] with sandstones, siltstones 

and mudstones (including a probable equivalent of the 

polhote marine Band), polbroc Burn [Ns 7293 1029] with 

conglomerate and sandstone including the polhote marine 

Band, and Kello water [Ns 730 104] with prominent 

kaolinitic beds. 


The base of the Clackmannan Group (undivided) is 

unconformable on the mainly greywacke sandstones of the 

ordovician Tappins and Barrhill groups. The top of the 

lower sequence is unconformably overlain by the cyclical 

sandstone, siltstone, mudstone, seatearth and coal of the 

basal scottish Coal measures Group (Figure 6, Column 5), 

whilst the top of the upper sequence is taken at the base of 

Tait’s marine Band (TmB) (davies, 1970) at the base of the 

scottish lower Coal measures Formation. 

Thickness 

The lower sequence is up to 10 m thick, whilst the upper 

sequence is up to 30 m thick. 


The lower sequence has been proved in the eastern part 

of the sanquhar Basin. it has not been encountered in 

boreholes in the centre and west of the basin. it possibly 

correlates with visean strata in the north of the Thornhill 

Basin namely the enterkin mudstone Formation (mcmillan, 

2002) or the lower limestone Formation of the midland 

valley (Browne et al., 1999). locally, the upper succession 

is limited to the western part of the sanquhar Basin. 

equivalents extend from the midland valley of scotland 

into the Thornhill Basin (mcmillan and Brand, 1995; 

smith, 1999; mcmillan, 2002). davies (1970) concluded 

that the bulk of the strata could be correlated with the upper 

part of the upper limestone Formation or the lower part of 

the passage Formation of the midland valley of scotland. 

subsequently, local erosion occurred and then deposition 

continued up into the langsettian, when Tait’s marine Band 

was deposited. 


The lower sequence is late visean, p 1 –p 2 ammonoid 

biozones (wilson in davies, 1970) or p 2 (Greig, 1971). 

The upper sequence is Arnsbergian to Kinderscoutian, 

e 2 –R 1 ammonoid biozones, on macrofaunal evidence, and 

pendleian (e 1 ) to langsettian, on microfloral evidence 

(davies, 1970). 

THORNHILL BASIN 

in the Thornhill Basin the Clackmannan Group comprises 

the enterkin mudstone and passage formations: 

73 

5.3.2 Enterkin Mudstone Formation (ENT) 

Name 

From enterkin Burn, north of Carronbridge, dumfries and 

Galloway. defined as a formation by mcmillan (2002; see 

also simpson and Richey, 1936). 

Lithology 

The formation consists dominantly of purple-grey mudstone 

and siltstone with interbedded sandstone. 


This mixed shelf carbonate and deltaic (‘Yoredale’) facies 

unit formed in a marine–intertidal environment. The 

mudstones contain a marine fauna. 

Stratotype 

The type section is in the enterkin Burn [Ns 8706 0526] 

where up to 15 m of interbedded red-brown and purple 

mudstone and siltstone, and purplish red sandstone and 

seatearth are exposed (mcmillan, 2002; simpson and 

Richey, 1936, table 3). 


The base of the formation is unconformable on the mainly 

sandstone-dominated turbidites of the ordovician Glenlee 

Formation, leadhills supergroup. 

The top of the formation is conformable with the base 

of the scottish lower Coal measures Formation (Figure 

6, Column 6) comprising sandstones, siltstones and mudstones, 

with seatearths. 

Thickness 

up to 15 m of the formation are exposed at the type section 

in the enterkin Burn [Ns 8706 0526] (mcmillan, 2002; 

simpson and Richey, 1936, table 3). 


The formation is restricted to the Thornhill Basin. The 

mudstones contain a fauna, that suggests possible correlation 

with the Clackmannan Group (undivided) visean strata of 

the sanquhar Basin. 


visean to Namurian (Brigantian to early pendleian). The 

mudstones contain a brachiopod, bivalve and nautiloid 

fauna, which may be of similar age to the fauna of the 

Closeburn limestone Formation. 

5.3.3 Passage Formation (PGP) 

Name 

From the passage Formation of the midland valley of 

scotland (see section 4.5.4 for full definition). details 

relevant to the Thornhill Basin are provided below. 

Lithology 

The sandstone facies includes grey, white and pink pebbly 

sandstone with beds of conglomerate. 

Stratotype 

partial type sections are defined at Towburn wood, 

Closeburn [NX 915 939] and in the BGs boreholes at 

Crichope linn (BGs Registration Number NX99Nw/1) 

[NX 9093 9551] and Carronbank (BGs Registration 

Number Ns80se/1) [Ns 8816 0127]. 




The base of the formation is apparently conformable, or 

disconformable, on the limestone and dolomitic limestone 

with interbedded sandstone, siltstone and mudstone of the 

Closeburn limestone Formation (Figure 6, Column 6), or 

unconformable on the mainly sandstone turbidites of the 

lower palaeozoic Glenlee Formation (ordovician) and 

Gala Group (silurian). 

The base of the nonmarine fossiliferous scottish lower 

Coal measures Formation conformably overlies the passage 

Formation, which lacks fossils. 

Thickness 

The maximum proved thickness is 43.9 m from 147.7 to 191.6 

m depth (based on mcmillan and Brand, 1995; mcmillan, 

2002) in the BGs Crichope linn Borehole (see above). 


The Thornhill Basin. equivalents occur in the midland valley 

of scotland and the western part of the sanquhar Basin. 


pre-westphalian. whilst there is no known fauna in the 

Thornhill Basin to provide a biostratigraphical age, the 

passage Formation in the midland valley of scotland is 

Namurian to westphalian (Arnsbergian to langsettian). 


see also Appendix 1. member of the passage Formation: 

5.3.3.1 TownBurn sanDsTone MeMBer (Twn) 

Name 

The Townburn sandstone member derives its name from 

its reference section (see Stratotype below). previous names 

include the Crichope sandstone member and passage 

Group (undivided). 

Lithology 

mainly medium- to coarse-grained sandstone with 

subsidiary conglomerate and pebbly sandstone. 


The member comprises fluvial-channel sands deposited in 

low sinuousity braided channels. (mcmillan, 2002, p. 74; 

Jones, 1994). 

Stratotype 

The type section is between 161.39 and 202.94 m depth in 

the Crichope linn Borehole (BGs Registration Number 

NX99Nw/1) [NX 9093 9551]. A reference section is the 

Town Burn, Townburn wood, Closeburn, 650 m northeast 

of Barraby Farm [NX 9146 9390]. mcmillan (2002, p. 

71) described this exposure as one of several localities in 

the Thornhill district where sequences up to 15 m thick of 

pebbly sandstone and beds of conglomerate can be seen (see 

also simpson and Richey, 1936). 


The lower boundary is unconformable on the mainly sandstone 

turbidites of the lower palaeozoic Glenlee Formation 

(ordovician) and Gala Group (silurian), though it rests 

locally on the lower Carboniferous limestone and dolomitic 

limestone with interbedded sandstone, siltstone and 

mudstone of the Closeburn limestone Formation, or the 

mudstone and siltstone with interbedded sandstone of the 

enterkin mudstone Formation. 

The base of the nonmarine fossiliferous scottish lower 

Coal measures Formation conformably overlies the fossil- 



74 

free Townburn sandstone member. 

Thickness 

some 41.55 m in the Crichhope linn Borehole (see above). 


Thornhill Basin at Closeburn, Keir, eccles, River Nith 

(drumlanrig), Hapland, Fellend, Townhead and morton 

wood. 

Age 

Namurian to westphalian. 

5.4 SCOTTISH COAL MEASURES GROUP 

(CMSC) 

The scottish Coal measures Group, as defined in full in 

section 4.6 is present in both the sanquhar and Thornhill 

basins, where it is again divided into lower, middle and 

upper formations. 

lithologically the group comprises a cyclical alternation 

of sandstone, siltstone and mudstone with coal seams well 

developed in the middle of the sequence. The rocks are typically 

grey, but they redden towards the top of the group as 

they approach the permian (variscan) unconformity. The 

lithofacies reflect steady basin subsidence in a generally 

deltaic environment with periodic marine incursions. Rare 

marine bands, Planolites bands and especially non-marine 

bivalve ‘musselbands’ are important for correlation. 

There is no formally defined lowstone marine Band 

equivalent at the base of the scottish Coal measures Group 

in these basins. in the western part of the sanquhar Basin 

the base is taken at the base of Tait’s marine Band (TmB), 

whilst in the east it occurs at an unconformity above the 

mainly sandstone, calcareous mudstone and siltstone of 

the older sequence of the Clackmannan Group (undivided). 

Generally in the Thornhill Basin the nonmarine fossiliferous 

scottish Coal measures Group overlies the nonfossiliferous 

sandstone facies of the passage Formation. The top 

of the group in both basins is the variscan unconformity. 

At sanquhar this is partially overlain by the olivine basalts 

of the lower permian Carron Basalt Formation, whilst in 

the Thornhill Basin the Carron Basalt Formation and red 

sandstones of the lower permian Thornhill sandstone 

Formation occur immediately above it. 

The maximum thicknesses of the scottish Coal measures 

Group in the southern uplands region are about 555 m in 

the sanquhar Basin and about 141 m in the Thornhill Basin. 

Based on the presence of nonmarine bivalve ‘musselbands’, 

both areas include strata of langsettian (westphalian A) to 

Bolsovian (westphalian C) age. 

The scottish Coal measures Group is also present in 

the stranraer Basin, and outcrops on the eastern side of 

the northern Rhins peninsula between Jamieson’s point 

[NX 032 711] and lochans [NX 060 572]. The sequence, 

formerly referred to the now obsolete leswalt Formation, 

comprises about 30 m of grey, red, and mottled yellowbrown 

sandstone, interbedded with purplish grey shale, 

rare seatclay, and a single pervasively weathered olivinebasalt 

sheet. The strata lie unconformably on steeply 

inclined lower palaeozoic greywackes, and become more 

arenaceous upwards. A flora from thin interbedded siltstones 

seems most likely to be of westphalian age, and the 

strata belong to either the scottish lower or middle Coal 

measures formations. The scottish upper Coal measures 

Formation appears to be missing here, so the upper boundary 

of the scottish Coal measures Group is considered

unconformable beneath beds of red sandstone and breccia 

of permian age (see stone, 1995, and references therein). 

5.4.1 Scottish Lower Coal Measures Formation (LCMS) 

Name 

From the lower Coal measures of the midland valley of 

scotland (see Browne et al., 1999; davies, 1970; Forsyth 

et al., 1996; mcmillan, 2002; mcmillan and Brand, 1995; 

simpson and Richey, 1936; smith, 1999; waters et al., 2007). 

Lithology 

in general, the formation comprises cyclical successions 

of sandstone, siltstone, mudstone, seatrock and coal. At 

sanquhar the lower parts of the formation are mainly 

arenaceous whilst the upper parts contain coals. 


Generally fluviodeltaic 

Stratotype 

Reference sections of the formation in the Thornhill Basin 

are provided by the BGs Crichope linn Borehole (BGs 

Registration Number NX99Nw/1) [NX 9093 9551] from 

98.0 to 147.7 m depth, and the BGs Carronbank Borehole 


from about 63 to 122 m depth. in the sanquhar Basin a 

reference section is at Kello water [Ns 734 106]. 


in the Thornhill Basin, the base of the nonmarine 

fossiliferous scottish lower Coal measures conformably 

overlies the nonfossiliferous sandstone facies of the passage 

Formation (Figure 6, Column 6). There is no formally 

defined lowstone marine Band equivalent, but in the BGs 

Crichope linn Borehole (see above) the base of the scottish 

lower Coal measures is taken below beds with Planolites 

sp., below the lowest nonmarine ‘musselband’. 

in the western part of the sanquhar Basin, where the 

formation overlies the Clackmannan Group (undivided) 

(Figure 6, Column 5), the local base of the scottish lower 

Coal measures is taken at the Tait’s marine Band (TmB) 

recognised by davies (1970), as here, again, there is no 

formally defined lowstone marine Band. 

where the scottish lower Coal measures overlie the 

former ‘Carboniferous limestone series’ (Clackmannan 

Group, undivided) in the eastern part of the sanquhar 

Basin, the boundary is unconformable. The irregular base, 

thickness and development of coals towards the base of the 

formation at sanquhar suggests that initial deposition of 

coal measures overstepped on to the northern margins of the 

southern upland massif. 

The top of the formation in both basins is conformable 

with the base of the scottish middle Coal measures 

and taken at the base of the vanderbeckei marine Band 

(vdmB). 

Thickness 

The maximum proved thickness of the formation is 50 m in 

the BGs Crichope linn Borehole (see above). At sanquhar, 

the succession is about 120 m thick. The thickness and 

development of coals within the formation at sanquhar is 

less than in the adjacent midland valley but greater than 

that around Thornhill. 


The formation is present in the Thornhill and sanquhar 

basins, where correlation with the midland valley of 

75 

scotland and solway Basin is on the basis of nonmarine 

‘musselbands’. 


langsettian (westphalian A) based on the presence 

of nonmarine ‘musselbands’ of the upper lenisulcata, 

communis and lower modiolaris biozones. while there is a 

lithological similarity with the successions elsewhere, the 

local bases of the formation are not strictly equivalent as the 

same basal marine band cannot be identified across the area. 

5.4.2 Scottish Middle Coal Measures Formation 

(MCMS) 

Name 

From the middle Coal measures of the midland valley of 



smith, 1999; simpson and Richey, 1936; waters et al., 

2007). 

Lithology 

in general, the formation consists of a cyclical sequence of 

sandstone, siltstone, mudstone, seatrock and coal. 


Generally fluviodeltaic. The widespread development of 

regular, well-developed coal seams suggests steady basin 

subsidence in a deltaic environment. 

Stratotype 

Type sections of the formation in the Thornhill Basin are 

defined in the BGs boreholes at Crichope linn (BGs 

Registration Number NX99Nw/1) [NX 9093 9551] from 

22.5 to 98.0 m depth, and Carronbank (BGs Registration 

Number Ns80se/1) [Ns 8816 0127] where the lower 45 m 

of the scottish middle Coal measures Formation are seen 

between about 18 and 63 m depth. A reference section in 

the sanquhar Basin is lagrae Burn [Ns 703 148], where 

sandstones and mudstones with seatearths and coals are 

seen. davies (1970) referred to former workings in the 

Calmstone and Creepie coals, mudstones with nonmarine 

bivalves and Estheria sp., and the Bankhead, eastside and 

skipsey’s (vanderbeckei) marine bands, the last mentioned 

including a fauna of brachiopods, molluscs and conodont 

elements. 


in both basins, the base of the scottish middle Coal 

measures conformably overlies the scottish lower Coal 

measures and is taken at the base of the vanderbeckei 

marine Band (vdmB) (Figure 6, Columns 5, 6). 

The top of the formation is conformable with the base 

of the scottish upper Coal measures and the boundary 

is taken at the base of the Aegiranum marine Band 

(AGmB). 

Thickness 

in the Thornhill Basin, the maximum proved thickness of 

the formation is 75.5 m in the BGs Crichope linn Borehole 

(see above). in the sanquhar Basin the formation is about 

135 m thick. 



basins, where correlation with the midland valley of 

scotland and solway Basin is on the basis of nonmarine 

‘musselbands’. 




duckmantian (westphalian B) based on the presence 

of nonmarine ‘musselbands’ of the upper part of the 

modiolaris and lower similis-pulchra biozones. 

5.4.3 Scottish Upper Coal Measures Formation (UCMS) 

Name 

From the upper Coal measures of the midland valley of 



simpson and Richey, 1936; smith, 1999; waters et al., 2007). 

Lithology 

in the Thornhill Basin the formation consists dominantly of 

purple and red siltstone and mudstone with thin sandstone 

and seatearth. in the sanquhar Basin the formation is fairly 

well developed and comprises mainly typical grey Coal 

measures beds with mudstones, siltstones and sandstones 

and subordinate thin coals in a succession that tends to be 

reddish towards the top. 

Stratotype 

The type section of the formation in the Thornhill Basin 

is defined in the BGs Borehole at Crichope linn (BGs 

Registration Number NX99Nw/1) [NX 9093 9551] between 

7.2 and 22.5 m depth. Reference sections in the sanquhar 

Basin are provided by lagrae Burn [Ns 707 141] and 

Tower Burn [Ns 754 122]. lagrae Burn shows mudstones, 

siltstones, sandstones, seatearths and thin coals, with faunas 

notably including nonmarine bivalves and Planolites 

ophthalmoides. The lagrae marine Band has foraminifers, 

Lingula mytilloides, Curvirimula sp. and Planolites 

ophthalmoides, and davies (1970, p. 77) suggested it may 

correlate with the standard edmondia marine Band of the 

pennine region. Tower Burn has sandstones, mudstones, 

and seatclays with thin coals. The phillipsi Biozone is 

represented there (simpson and Richey, 1936). 


The base of the scottish upper Coal measures in both 

basins conformably overlies the scottish middle Coal 



76 

measures and is taken at the base of the Aegiranum marine 

Band (AGmB) (Figure 6, Columns 5, 6). 

The top of the formation in both basins is the variscan 

unconformity. At sanquhar this is partially overlain by 

the olivine basalts of the typically much weathered lower 

permian Carron Basalt Formation, whilst in the Thornhill 

Basin the Carron Basalt Formation and red sandstones of 

the lower permian Thornhill sandstone Formation occur 

immediately above it. The reddening towards the top of 

the formation here may be due to oxidation below the prepermian 

erosion surface or staining by waters percolating 

from the subsequent permian overburden. 

Thickness 

in the Thornhill Basin the maximum proved thickness of 

the formation is 15.3 m in the BGs Crichope linn Borehole 

(see above). The remaining thickness of the formation in the 

sanquhar Basin is estimated to be up to 300 m. 



basins. in the Thornhill Basin, correlation with the midland 

valley of scotland and solway Basin is based on the 

presence of mudstone with Planolites ophthalmoides 

and abundant foraminifers, or Lingula mytilloides, which 

is taken to represent the Aegiranum marine Band. At 

sanquhar, the formation lies within the core of the basin 

and was cut out by later movement on the southern upland 

Fault. it too correlates with similar strata in the midland 

valley of scotland (and southwards to Thornhill and 

beyond) based on the presence of Planolites opthalmoides 

and non-marine bivalves of the upper similis-pulchra 

Biozone. 


Bolsovian (westphalian C). in the Thornhill Basin, 

the Aegiranum marine Band (AGmB) is taken to be 

represented by mudstone with Planolites ophthalmoides 

and abundant foraminifers, or Lingula mytilloides. The 

trace fossil Planolites ophthalmoides and nonmarine 

bivalves of the upper similis-pulchra Biozone are present 

at sanquhar.

6 Carboniferous rocks of the Northern england province 

6.1 INTRODUCTION 

The Northern england province encompasses the area 

between the southern uplands and the Craven Fault system 

(Figure 3); it includes the Northumberland and stainmore 

troughs, the Tweed and solway basins, the Alston and 

Askrigg blocks and the manx–lake district Block (Figures 

7–15). during westphalian times this area formed the 

northern part of the pennine Basin. 

The Northumberland Trough has a Tournaisian succession 

distinct from the rest of the province. Along the 

southern margin of the southern uplands massif, the earliest 

Carboniferous strata are of continental and peritidal 

facies, very similar to the inverclyde Group of the midland 

valley of scotland. This group name and some component 

formations have been extended into the northern part of 

the Northumberland Trough. within the Northumberland 

Trough the inverclyde Group is overlain by the Border 

Group of early visean age. 

elsewhere, the continental and peritidal facies ‘cornstone’ 

subfacies is preserved only in local basins in the deformed 

lower palaeozoic rocks that formed the devonian continental 

landmass. The distribution, adjacent to the pennine–dent 

and lake district boundary faults suggests that they were preserved 

in half-grabens that formed during the initial stages of 

extension in the late devonian–early Carboniferous. local 

formation names are used for each isolated basin. The continental 

and peritidal facies ‘cementstone’ subfacies is associated 

with deposition in epicontinental basins with a limited 

marine influence. The evaporite-bearing succession marks 

the initial marine transgression with deposition in sabkha 

environments along arid shorelines. An increasing marine 

influence and transgression is denoted by the deposition of 

peritidal carbonates. only within the stainmore Trough has 

sufficient lithostratigraphical variation been identified to 

warrant continental and peritidal facies strata being assigned 

to a group, namely the Ravenstonedale Group. 

south of the Northumberland Trough, the remainder of the 

province comprised basins and highs both of which formed 

largely distinct and isolated areas of deposition until Asbian 

times, each with different formational nomenclature. However, 

each structural entity showed a consistent development in 

facies in time from open marine, platform and ramp carbonates 

facies to cyclical mixed shelf carbonate and deltaic (‘Yoredale’) 

facies. strata of the former are assigned to the Great scar 

limestone Group and strata of the latter to the yoredale Group. 

during Namurian times, the millstone Grit Group (fluviodeltaic 

(‘Millstone Grit’) facies) extended over the Askrigg Block, 

and subsequently, during westphalian times the pennine 

Coal measures Group (fluviodeltaic (‘Coal Measures’) facies) 

extended across the entire province. ‘Barren measures’ (alluvial 

(‘Barren Measures’) facies) of late westphalian age, have been 

assigned formation names within the warwickshire Group. 

6.2 UNGROUPED FORMATIONS OF 

CONTINENTAL AND PERITIDAL FACIES IN THE 

CRAVEN BASIN 

The late devonian to visean continental and peritidal facies is 

restricted to localised areas of deposition at the northern margin 

77 

of the Craven Basin. The deposits have been attributed a standalone 

formational name, with a geographical range limited to 

the known extent of the sub-basin. The sFC Committee did not 

consider these isolated deposits warranted group status. 

6.2.1 Stockdale Farm Formation (STFA) 

Name 

The formation is named after stockdale Farm, stockdale, 

east of settle. it was first proposed by Arthurton et al. 

(1988) for a succession proved in the Halsteads (Cominco 

s2) Borehole (BGs Registration Number sd86sw/6) [sd 

8491 6345] and the stockdale Farm (Cominco s7) Borehole 

(BGs Registration Number sd86se/6) [sd 8541 6378], 

both of which are located on the settle sheet. 

Lithology 

The formation comprises an informal lower member of thinly 

interbedded laminated dolostone, dolomitic–siliciclastic 

siltstone, mudstone and laminated anhydrite, which is 

overlain by an informal middle member of interbedded 

sandstone, siltstone, mudstone and thin limestone. The 

sandstones are arkosic pale grey, fine-grained, micaceous 

and carbonaceous, and the limestones are dark grey micrites 

with subordinate packstones and wackestones. An upper 

informal member comprises interbedded limestone, siltstone 

and mudstone, lithologically similar to the middle member, 

but lacking sandstones. 


Alluvial plain and marginal marine flats subject to periodic 

desiccation and fluctuating salinity, in a semi-arid climate. 

Stratotype 

The type section of the formation is the Halsteads (Cominco 

s2) Borehole (see above) from about 389.35 m to the 

base of the bore at 426.35 m depth. A reference section, 

proving the upper and middle parts of the formation, is the 

stockdale Farm (Cominco s7) Borehole (see above) from 

about 169.9 m to the base of the bore at 309.9 m depth. 


The base of the formation is not seen, but it is possibly an 

angular unconformity above lower palaeozoic sandstone, 

siltstone and mudstone. 

The top of the formation is a deeply fissured surface 

marking a significant non-sequence. it is overlain by 

conglomerates of the Chapel House limestone Formation 

and underlain by limestone, siltstone and mudstone of the 

stockdale Farm Formation (Figure 15, Column 6). 

Thickness 

Known only in boreholes (see above), the formation is 

greater than 165 m thick. 


The formation occurs in the Askrigg Block–Craven 

Basin ‘Transition Zone’. it is possibly equivalent to the 

Roddlesworth Formation of the Central lancashire High 

(see waters et al., 2009). 




Tournaisian to Chadian. The macrofauna is generally 

poor except in the top 12 m where it includes Delepinea 

sp. and Michelinia megastoma (see Arthurton et al., 

1988). The topmost 11 m of the formation include the 

typical early Chadian (Tournaisian) foraminifers 

Palaeospiroplectammina mellina, Endothyra danica, 

Lugtonia monilis and Spinoendothyra mitchelli (Arthurton 

et al., 1988). 


Arthurton et al. (1988) proposed three members, in 

ascending order: the Halsteads shales-with-Anhydrite, 

stockdale Farm sandstones and shales, and stockdale Farm 

limestones and shales. This nomenclature is unacceptable 

as two of the members duplicate the name of the formation 

and the lithological epithets are unsuitable. As these units 

are recorded only in the subsurface, no attempt has been 

made during this study to formalise the definition of these 

units as members. 

6.3 INVERCLYDE GROUP (INV) 

The inverclyde Group (paterson and Hall, 1986) (Figure 7) 

of continental and peritidal facies comprises strata directly 

equivalent to the group of the same name present in the 

midland valley of scotland (see section 4.2 above), 

where the type area occurs at Greenock in the inverclyde 

district (see paterson and Hall, 1986). The Kinnesswood 

and Ballagan formations also equate to their namesakes in 

the midland valley of scotland, but in the Berwick area 

and solway Basin they are separated by the Kelso and 

Birrenswark volcanic formations respectively (see Greig, 

1988 and lumsden et al., 1967). There is no equivalent to 

the Clyde sandstone Formation of the midland valley of 

scotland in the Northern england province. 

The base of the group is taken where silurian strata 

(greywackes with interbedded mudstones) of the Riccarton 

Group are succeeded unconformably by red sandstones, siltstones 

and conglomerates of the Kinnesswood Formation. 

The base of the Border Group (heterolithic clastic and 

nonmarine carbonate facies and fluviodeltaic (‘Millstone 

Grit’) facies) defines the top of the group (see section 6.5). 

Tournaisian (Courceyan to Chadian) in age, the 

inverclyde Group is up to 900 m thick in the Tweed valley, 

Northumberland, and up to 640 m thick in the solway Firth 

area. 

6.3.1 Kinnesswood Formation (KNW) 

Name 

From the Kinnesswood Formation of the midland valley 

of scotland. see section 4.2.1 for definition. The 

following description is specific to the Northern england 

province. 

Lithology 

The Kinnesswood Formation comprises red sandstones, 

siltstones and conglomerates. 


The original sediments were laid down in calcrete-rich 

(‘cornstone’) alluvial fans that were deposited in a series of 

small, linked basins with internal drainage that developed 

during early stages of crustal extension (Chadwick et al., 

1995). The beds are dominantly fluvial with a palaeocurrent 

towards the north-east. 



78 

Stratotype 

The type section is defined in the midland valley of 

scotland (see section 4.2.1). 


The base of the formation is unconformable upon silurian 

strata (grewackes and interbedded mudstones) of the 

Riccarton Group. 

in the Berwick area and solway Basin, the mainly basalts 

of the Kelso and Birrenswark volcanic formations overlie 

the formation conformably and irregularly respectively 

(Figure 8, Column 12; Figure 6, Column 7). 

Thickness 

up to 200 m. 


The formation extends across and south of the southern 

uplands from eyemouth to dalbeattie, where it crops out 

narrowly along the northern margin of the Northumberland 

Trough in the langholm area (lumsden et al., 1967) and 

west of the Cheviot Hills. 

Age 

late devonian (Famennian) to early Tournaisian (Courceyan). 

lumsden et al. (1967) and George et al. (1976) postulated an 

early Carboniferous age for the upper part of the formation. 

6.3.2 Kelso Volcanic Formation (KT) 

Name 

Named after the town of Kelso, with early references to the 

‘Kelso traps’ (see eckford and Ritchie, 1939) and Kelso 

lavas (mcRobert, 1925). 

Lithology 

The Kelso volcanic Formation comprises olivine basalts 

and subordinate tuffs and sedimentary strata (volcaniclastic 

sandstone). 


The formation formed during the main initial phase of 

extensional faulting associated with development of the 

Northumberland Trough. 

Stratotype 

partial type sections occur in the Blackadder water at 

lintmill [NT 7338 4636] (which includes the lowest lava), 

lintmill Railway Cutting [NT 727 463 to 736 466] east of 

Greenlaw (see williamson in stephenson et al., 2003), the 

eden water below Girrick [NT 6676 3724], and the River 

Tweed south of makerstoun House [NT 6736 3154]. see 

eckford and Ritchie (1939) for further reference to these 

local sequences in the formation. 


The base of the formation conformably overlies the red 

sandstones, siltstones and conglomerates of the Kinneswood 

Formation in Berwickshire (Figure 8, Column 12). 

The top of the formation is conformable with the base of 

the ‘cementstone’-bearing strata of the Ballagan Formation. 

Thickness 

up to 150 m. 


Berwickshire. Correlated with the Birrenswark volcanic 

Formation of the solway Basin.

Groups and main lithofacies Groups and formations Chronostratigraphy 

Volcanic rock lithofacies 

v v 

NORTHUMBERLAND 

TROUGH & 


TROUGH & 

SOLWAY BASIN 

ASKRIGG 

BLOCK 

NORTH & WEST 

CUMBRIA 

SOLWAY BASIN 

ASKRIGG 

BLOCK 

NORTH & WEST 

CUMBRIA 

Barren Measures lithofacies 

ASTURIAN 

CHEVIOT BLOCK 

& NORTH-EAST 

NORTHUM- 

BERLAND 

PENNINE 

UPPER 

COAL 

MEASURES 

FORMATION 

WHITEHAVEN 

SANDSTONE 

FORMATION 

PUCM Fm 

PENNINE 

MIDDLE 

COAL 

MEASURES 

PENNINE 

MIDDLE 

COAL 

MEASURES 

PENNINE 

MIDDLE 

COAL 

MEASURES 

FORMATION 

PENNINE 

LOWER 

COAL 

MEASURES 

FORMATION 

PENNINE COAL MEASURES 

FORMATION 

PENNINE 

LOWER 

COAL 

MEASURES 

FORMATION 

PENNINE 

LCM 

FORMATION 

PENNINE 

MCM Fm 

PENNINE 

LOWER 

COAL 

MEASURES 

FORMATION 

PENNINE 

MCM Fm 

PENNINE 

LOWER 

COAL 

MEASURES 

FORMATION 

FORMATION 

PENNINE 

LOWER 

COAL 

MEASURES 

FORMATION 

ROSSENDALE 

FORMATION 

STAINMORE 

FORMATION 

MARSDEN 

FORMATION 

HEBDEN 

FORMATION 

STAINMORE 

FORMATION 

STAINMORE 

FORMATION 

STAINMORE 

FORMATION 

STAINMORE 

FORMATION 

YOREDALE GROUP 

YOREDALE GROUP PENNINE COAL MEASURES GROUP 

WARWICKSHIRE GROUP 

WARWICKSHIRE Gp 

CHEVIOT BLOCK 

& NORTH-EAST 

NORTHUM- 

BERLAND 

WARWICK- 

SHIRE 

GROUP 

WARWICK- 

SHIRE 

GROUP 


WESTPHALIAN 

BOLSOVIAN 

STAINMORE 

TROUGH 

PENNINE 

COAL 

MEASURES 

GROUP 

PENNINE COAL MEASURES Gp 

STAINMORE 

TROUGH 


DUCKMAN- 

TIAN 

ALSTON 

BLOCK 

PENNINE 

COAL 

MEASURES 

GROUP 

ALSTON 

BLOCK 

PCM Gp 

PCM GROUP 

PCM GROUP 

PENNINE 

COAL 

MEASURES 

GROUP 

PENNINE 

COAL 

MEASURES 

GROUP 

PENNINE 

COAL 

MEASURES 

GROUP 


LANGSET- 

TIAN 

PENNINE 

COAL 

MEASURES 


YEADONIAN 

YOREDALE Gp 

YOREDALE 

GROUP 

Platform/ramp carbonate lithofacies 

MARSDEN- 

IAN 

MILLSTONE 

GRIT 

GROUP 

Heterolithic clastic and nonmarine 

carbonate lithofacies 

KINDER- 

SCOUTIAN 

NAMURIAN VISEAN TOURNAISIAN 

ALPORTIAN 



SAMLESBURY 

FORMATION 

SILSDEN 

FORMATION 

MILLSTONE GRIT GROUP 

YOREDALE 

GROUP 

YOREDALE 

GROUP 

YOREDALE 

GROUP 

YOREDALE 

GROUP 


CHOKIERIAN 

PENDLETON Fm 

79 

STAINMORE 

FORMATION 

YOREDALE Gp 

STAINMORE 

FORMATION 

ALSTON 

FORMATION 

ALSTON 

FORMATION 

ALSTON 

FORMATION 

ALSTON 

FORMATION 


ALSTON 

FORMATION 

YOREDALE Gp 

YOREDALE Gp 

TYNE 

LIMESTONE 

FORMATION 

TYNE 

LIMESTONE 

FORMATION 

MELMERBY 

SCAR 

LIMESTONE 

FORMATION 

KNIPE SCAR 

LIMESTONE 

FORMATION 

POTTS BECK 

FORMATION 

DANNY 

BRIDGE 

LIMESTONE 

FORMATION 

GARSDALE 

LIMESTONE 

FORMATION 

ESKETT 

LIMESTONE 

FORMATION 

CRAVEN Gp MILLSTONE GRIT Gp 

Non-sequence 

ARNSBERG- 

IAN 

FURNESS & 

CARTMEL 

MILLSTONE 

GRIT 

GROUP 

FURNESS & 

CARTMEL 

STAINMORE 

FORMATION 

YOREDALE 

GROUP 

PENDLEIAN 

PENDLETON 

FORMATION 

BOWLAND 

SHALE 

MILLSTONE 

GRIT 

GROUP 

CRAVEN 

ALSTON 

Fm 

BRIGANTIAN 

ALSTON 

FORMATION 

YOREDALE 

GROUP 

YOREDALE 

GROUP 

YOREDALE 

GROUP 

ASBIAN 

HOLKERIAN 

MARSETT 

FORMATION 

ASHFELL 

LIMESTONE 

FORMATION 

FAWES WOOD 

LIMESTONE 

FORMATION 

FELL 

SANDSTONE 

FORMATION 

BORDER GROUP 

FELL 

SANDSTONE 

FORMATION 

BORDER GROUP 

GREAT SCAR LMST GROUP 

ASHFELL 

SANDSTONE 

ASHFELL 

SANDSTONE 

ARUNDIAN 

FORMATION 

FORMATION 

LYNE 

FORMATION 

RAVENSTONEDALE 

GROUP 

BALLAGAN 

FORMATION 

BALLAGAN 

FORMATION 

BREAKYNECK 

SCAR LMST 

FORMATION 

BROWNBER Fm 

SCANDAL 

BECK LMST Fm 

COLDBECK Fm 

STONE GILL 

LMST Fm 

GREAT SCAR LIMESTONE GROUP 


FRIZINGTON 

LIMESTONE 

FORMATION 

TOM CROFT 

LIMESTONE Fm 

PENNY FARM 

GILL Fm 

MARSETT Fm 


URSWICK 

LIMESTONE 

FORMATION 

PARK 

LIMESTONE 

FORMATION 

DALTON Fm 

RED HILL 

LIMESTONE Fm 


GREAT 

SCAR 

LIMESTONE 

GROUP 

GREAT 

SCAR 

LIMESTONE 

GROUP 

v 

v 

GREAT 

SCAR 

LIMESTONE 

GROUP 

GREAT 

SCAR 

LIMESTONE 

GROUP 

BORDER 

GROUP 

GREAT 

SCAR 

LIMESTONE 

GROUP 

GREAT 

SCAR 

LIMESTONE 

GROUP 

RAVENSTONE- 

DALE Gp 

BORDER 

GROUP 

GREAT 

SCAR 

GREAT 

SCAR 

LIMESTONE 

GROUP 

CHADIAN 

MARSETT 

FORMATION 

RAYDALE 

DOLOSTONE 

FORMATION 

COURCEYAN 

KELSO 

VOLCANIC 

FORMATION 

KINNESS- 

WOOD 

FORMATION 


BIRRENSWARK 

VOLCANIC Fm 

PINSKEY GILL 

KINNESS- 

WOOD 

FORMATION 


RAVENSTONEDALE Gp 

MARTIN 

LIMESTONE 

FORMATION 

MARSETT 

FORMATION 

LIMESTONE 

GROUP 

GREAT 

SCAR 

LIMESTONE 

INVERCLYDE 

GROUP 

INVERCLYDE 

GROUP 


GROUP 

MARSETT 

FORMATION 

RAVEN- 

STONE- 

DALE 

RAVENSTONE- 

DALE Gp 

v 

FAMENNIAN 

COCKERMOUTH 

VOLCANIC 

FORMATION 


GROUP 


GROUP 

v v v v 

GROUP 

INVERCLYDE 

GROUP 

INVERCLYDE 

GROUP 

RAVENSTONE- 

DALE Gp 

RAVENSTONE- 

DALE Gp 

Figure 7 lithostratigraphical 

nomenclature for the Northern 

england region. see section 3 

for description of lithofacies, 

and Figures 8, 9, 11–15 for 

other localities discussed in 

text. This figure is not intended 

to name all the formations in 

the region. Fm formation; Gp 

group; lCm lower Coal 

measures; lmsT limestone; 

mCm middle Coal measures; 

pCm pennine Coal measures; 

puCm pennine upper Coal 

measures. 



12 

NORTHEAST 


GL 

PENNINE UPPER 

COAL MEASURES 

FORMATION 

11 

NORTHWEST 


10 

CANONBIE 

ALSTON 

FORMATION 

PENNINE 

MIDDLE COAL 

MEASURES 

FORMATION 

PENNINE 

COAL 

MEASURES 

GROUP 

‘BECKLEES 

SANDSTONE 

FORMATION’ 



PENNINE UPPER 

COAL MEASURES 

FORMATION 

ISLE OF MAN 

WTLL 


SBMB 

PENNINE LOWER 

COAL MEASURES FM 

M 

VDMB 

M 

‘CANONBIE BRIDGE 

SANDSTONE 

FORMATION’ 

STAINMORE 

FORMATION 

GL 

‘ESKBANK WOOD 

FORMATION’ 

WARWICKSHIRE 

GROUP 

PENNINE 

LOWER COAL 

MEASURES 

FORMATION 

ALSTON 

FORMATION 

CAMB 

SFMB 

EMMB 

AGMB 

SOMB 

HTMB 

8 9 

SOUTH NORTH 

VDMB 

M 

M 

M 

M 

M 

M 

PENNINE MIDDDLE 


M 

TYNE 

LIMESTONE 

FORMATION 

PGL / LTL 

PENNINE 

LOWER COAL 


PENNINE COAL 

MEASURES GP 

PENNINE COAL 

MEASURES GP 

PENNINE LOWER 

COAL MEASURES 

SBMB 

FORMATION 

ROSSENDALE FORMATION 

CRAVEN 

GROUP 

GREAT SCAR 

LIMESTONE 

GROUP 

ALSTON FORMATION/ 

BALLADOOLE FORMATION 

(not exposed) 

MILLSTONE GRIT 

GROUP 

SCARLETT 

POINT MEMBER 

HODDERENSE 

LIMESTONE 

FORMATION GREAT SCAR 

KNOCKRUSHEN LIMESTONE 

FORMATION 

GROUP/ 

LANGNESS 

YOREDALE 

CONGLOMERATE GROUP 

FORMATION 

SCARLETT VOLCANIC 

v MEMBER v 

BOWLAND 

SHALE FORMATION 

BALLADOOLE 

FM 


DERBYHAVEN FM 

FELL 

SANDSTONE 

FORMATION 

BORDER GROUP 

STAINMORE 

FORMATION 

YOREDALE GROUP PENNINE COAL MEASURES GROUP 

SBMB 

M 

M 

LONAN FORMATION 

MANX 

GROUP 


GROUP 

80 

TYNE 

LIMESTONE 

FORMATION 

BALLAGAN 

FORMATION 

LOCALITIES 

N 

SCALE 

KELSO 

VOLCANIC 

FORMATION 

v 

KINNESSWOOD 

FORMATION 


400 

12 

10 

200 

metres 

11 

CTB / KBL 

FELL 

SANDSTONE 

FORMATION 

9 

0 

8 

LYNE 

FORMATION 

BORDER GROUP 

98001783 

BALLAGAN 

FORMATION 

INVERCLYDE 

GROUP 

Figure 8 Generalised vertical sections and correlation for Carboniferous strata in the isle of man, Canonbie and Northumberland. Based on Ramsbottom et al. (1978) and 

Chadwick et al. (2001). The profiled location of the numbered sections is given in the inset map. see Appendices 1 and 2 for the names of the lithostratigraphical units 

shown by BGs lexicon of Named Rock units computer codes. m marine band; v indicates named volcanic rock units; blue colour indicates named limestone beds; wavy 

lines indicate unconformity surfaces.

Age 

mid Tournaisian (Courceyan) 

6.3.3 Birrenswark Volcanic Formation (BIRV) 

Name 

Named from Birrenswark (Burnswark) Hill. described in 

detail by pallister (1952). see also lumsden et al. (1967); 

lintern and Floyd (2000). 

Lithology 

The Birrenswark volcanic Formation comprises olivine 

basalt lavas intercalated with subordinate tuffs and 

impersistent sedimentary strata including sandstone, 

mudstone and dolostone (‘cementstone’). 


The formation formed during the main initial phase of 

extensional faulting associated with development of the 

Northumberland Trough. 

Stratotype 

partial type sections occur near langholm at white Cove 

[Ny 4060 9176] where almost the total sequence about 

15 m thick is seen, warb law [Ny 359 831] where at least 

five flows about 60 m thick in total occur, and Hartsgarth 

Fell at the head of the Tarras water [Ny 446 935] where 

the base of the sequence and upwards through about 29 m 

is seen (see lumsden et al., 1967, pp. 73–76). 


The irregular base of the formation overlies the ‘cornstone’bearing 

Kinnesswood Formation in the solway Basin 

(Figure 6, Column 7; Figure 10, Columns 2, 3). 

The top of the formation is the faulted or irregularly 

conformable base of the ‘cementstone’-bearing strata of the 

Ballagan Formation. 

Thickness 

Between 15 and 60 m. Best developed between dinely and 

langholm, the lavas thin westwards towards Birrenswark 

Hill. 


solway Basin. From between dinely and langholm 

westward to Kirkbean Glen, southern Kirkcudbrightshire. 

Correlated with the Kelso volcanic Formation. 

Age 

mid Tournaisian (Courceyan). 

6.3.4 Cottonshope Volcanic Formation (COVO) 

Name 

previously known as the Cottonshope lavas (Taylor et al., 

1971). 

Lithology 

Basalt lavas, olivine-phyric, tholeiitic; several sheets of 

intensely fractured, dark blue-grey basalt, each passing 

up into highly amygdaloidal, scoriaceous and pillow-like 

tops which contain infills of overlying sedimentary rock. 

The upper part of formation is intercalated with dark grey 

and greenish grey sandstone and argillaceous dolostone 

(‘cementstone’) of the overlying Ballagan Formation. 

Stratotype 

The type section is Cottonshope Head Quarry and adjacent 

Cottonshope Burn, upper Redesdale, Northumberland [NT 

81 

803 058] (see millward in stephenson, et al., 2003; miller, 

1887; Tomkeieff, 1931; Taylor et al., 1971). Here the 

volcanic succession comprises three sheets of basalt. The 

lowest one is 12 m thick and has an undulating pillow-like 

to ‘slaggy’, scoriaceous top with sedimentary infills. This 

is overlain by a 6 m-thick vesicular basalt. The uppermost 

basalt, also 6 m thick, is separated from the underlying 

ones by 6 m of bedded mudstones, flaggy sandstones and 

‘cementstones’ (millward in stephenson, et al. (2003, 

p. 136). 


The lower boundary is taken at the broadly conformable 

base of the lowest basalt sheet that sharply overlies a 

sequence of red and grey flaggy sandstones with ochreous 

brown spots, interbedded with purple, red, lilac and green 

mudstone containing ochreous concretions, and thin 

concretionary carbonate (‘cornstone’) beds (the lower 

Freestone Beds of Taylor et al., 1971). This is possibly part 

of the Kinnesswood Formation. 

The upper boundary of the formation is taken at the 

base of the overlying interbedded sandstone, mudstone and 

argillaceous dolostone sequence of the Ballagan Formation 

(formerly the Cementstone Group). The upper contact is 

intercalated. 

Thickness 

up to 24 m. 


south-west flanks of the Cheviot Block: exposed in 

Cottonshope Burn, spithope Burn, Hungry law, and 

between the Bareinghope Burn and the Chattlehope Burn, 

Northumberland. 

Age 

Tournaisian. 

6.3.5 Roddam Dene Conglomerate Formation (RDCO) 

Name 

Named after the type section (see Stratotype below) (Cossey 

et al., 2004). 

Lithology 

Conglomerate, in thick and very thick beds; reddish coloured; 

subangular to subrounded clasts of pebble- to boulder-grade 

set in a clay-rich sandstone matrix; matrix supported to 

clast supported. Clasts predominantly of andesite, derived 

from the Cheviot volcanic Formation, but also rare clasts 

of silurian mudstone and greywacke sandstone and Cheviot 

granite. There are minor intercalations of mudstone, 

sandstone and siltstone at the top. 

Stratotype 

The type section is Roddam dene, south of wooler, 

Northumberland [Nu 018 207 to 025 207] where about 170 m 

of dominantly conglomerate, with interbedded sandstone, 

mudstone, and calcareous mudstone are seen in three faultbounded 

units (see Cossey et al., 2004, pp. 149–151). 


The lower boundary is not seen, but it is thought to overlie 

the Cheviot volcanic Formation unconformably. 

The upper boundary of the formation is not seen, but 

it is believed to be overlain conformably by rocks of the 

Ballagan Formation (formerly the Cementstone Group of 

Northumberland). 



Thickness 

About 170 m seen. 


limited to the eastern flanks of the Cheviot Block, 


Age 

Tournaisian. 

6.3.6 Ballagan Formation (BGN) 

Name 

From the Ballagan Formation of the midland valley of 

scotland. see section 4.2.2 for definition. The formation 

now encompasses part of the Cementstone Group of 

previous literature in Northern england, the Tweed Basin, 

and the solway Basin (see peach and Horne, 1903; Craig, 

1956; Craig and Nairn, 1956; Nairn, 1956, 1958), and part 

of the lower Border Group of lumsden et al. (1967). The 

following description is specific to the Northern england 

province. 

Lithology 

The Ballagan Formation comprises interbedded sandstone, 

mudstone, limestone (‘cementstone’) and anhydrite, the latter 

present in the subsurface only. There are also pseudomorphs 

after evaporite minerals, some rootlet beds and thin coals. 

in the langholm and Annandale districts, the Kirkbean 

Cementstone member includes the whita and Annandale 

sandstone beds respectively. The former comprises medium- 

to thickly bedded, fine- to coarse-grained, white, grey 

and pink sandstones with a few thin siltstones and sandy 

‘cementstones’, and the latter, dark red, fine- to coarsegrained 

sandstone and locally derived conglomerate. 


deposition of the formation was dominated by the influx 

of alluvial fans, and fluvial and fluviodeltaic sediments 

from the southern uplands, intercalated with lacustrine 

and arid coastal plain deposits (deegan, 1973; leeder, 

1974). Hypersaline lacustrine and floodplain facies include 


and thin coals. The whita and Annandale sandstone beds 

are fluviodeltaic sedimentary rocks locally derived from 

the north to north-west in the southern uplands massif 

(leeder, 1974). 

Stratotype 

The type section is defined in the midland valley of 

scotland. partial type sections include: the whita sandstone 

Beds of langholm in disused quarries on whita Hill [Ny 

381 848], and in the River esk from longwood [Ny 3710 

8290] to Broomholm [Ny 3730 8150]; the Annandale 

sandstone Beds on the River Annan from Rochell [Ny 

1300 7450] to Hoddom Castle [Ny 1500 7300]; the 

Kirkbean Cementstone member in the Tarras water [Ny 

3811 8119] and at Kirkbean Glen [NX 9745 5914]; and 

the orroland member in the coastal section from port 

mary [Ny 7520 4540] to Castle muir [Ny 7980 4700]. A 

reference section for the Kirkbean Cementstone member 

is the BGs Hoddom No.2 Borehole (BGs Registration 

Number Ny17se/3) [Ny1641 7285] between 139.84 and 

199.74 m depth (end of borehole). 


The base of the formation is faulted or irregularly 

conformable upon the Birrenswark volcanic Formation in 



82 

the solway Basin (Figure 6, Column 7; Figure 10, Columns 

2, 3), conformable on the Kelso volcanic Formation in 

the Berwick area (Figure 8, Column 12), and elsewhere 

unconformable upon devonian and older strata. 

The top of the formation is at least presumed conformable 

beneath the cyclical sequences of sandstone, siltstone, 

mudstone and thin-bedded limestone of the lyne Formation 

(Border Group) of the Northumberland Trough and solway 

Basin (Figure 6, Column 7; Figure 10, Columns 2, 3), but is 

unconformable beneath the sandstone of the Fell sandstone 

Formation in the north-east part of the Northumberland 

Trough (Figure 8, Column 12; Figure 11, Column 1; 

Figure 12, Columns 1, 2; Figure 13, Column 3). 

Thickness 

The ‘cementstone’ facies is up to 250 m thick in the 

Northern england province. The whita sandstone in the 

langholm district is about 300 m thick (lumsden et al., 

1967, p. 78). The Annandale sandstone Beds in the dalton 

area of dumfriesshire are 180 m thick. 


The formation crops out in the north-eastern margins of 

the Northumberland Trough and at Kirkbean in the solway 

Firth area. in the central part of the Northumberland Trough 

a lateral facies change sees the Ballagan Formation pass 

into the lyne Formation of the Border Group. 


Tournaisian (Courceyan to Chadian) (Armstrong and 

purnell, 1987). Characterised by bivalves (including a 

modiolid fauna) and Serpula sp. 


see also Appendix 1. members of the Ballagan Formation 


6.3.6.1 KirKBean CeMenTsTone MeMBer (KiCM) 

Name 

previously named the ‘Basal Cementstones’ by Craig 

(1956), and the Kirkbean Cementstone Formation by 

lintern and Floyd (2000), the status is here changed to a 

member. 

Lithology 

The Kirkbean Cementstone member comprises mainly 

thinly interbedded greenish grey carbonaceous siltstone 

and argillaceous limestone (‘cementstone’). in the 

langholm and Annandale districts, it includes the whita 

and Annandale sandstone beds respectively. The former 

comprise medium- to thickly bedded, fine- to coarsegrained, 

white, grey and pink sandstones with a few 

thin siltstones and sandy ‘cementstones’, and the latter 

comprise dark red, fine- to coarse-grained sandstone and 

locally derived conglomerate. 

Stratotype 

The partial type section is Kirkbean Glen [NX 9745 5914] 

where fragmentary plant remains, but no shelly fauna, have 

been found in a 20 m sequence of carbonaceous siltstones 

and mudstones with thin ‘cementstone’ stringers, that is 

faulted against basalt (lintern and Floyd, 2000, p. 77). 


The base rests unconformably on basalt lavas of the 

Birrenswark volcanic Formation (Figure 10, Column 2). 

The top of the member is not exposed, but is probably 

gradational with the southerness limestone member.

Thickness 

The ‘cementstone’ facies is greater than 100 m thick. The 

whita sandstone in the langholm district is about 300 m thick 

(lumsden et al., 1967, p. 78), and the Annandale sandstone 

Beds in the dalton area of dumfriesshire are 180 m thick. 


Kirkbean area, southerness, Kirkcudbrightshire, dumfries 

and Galloway. 

Age 

Tournaisian (Courceyan to Chadian). 

6.3.6.2 wall Hill MeMBer (wlH) 

Name 

previously named the wall Hill sandstone Group by 

deegan (1973), and the wall Hill sandstone Formation by 

lintern and Floyd (2000). The status is here changed to a 

member and the ‘sandstone’ epithet dropped. 

Lithology 

The member comprises fining-upwards cycles of pale grey 

to white conglomerates and sandstones with thin purple 

siltstones, ‘marls’ and shales. 

Stratotype 

The type section is the coastal outcrop between white 

port Bay [NX 7234 4336] and port mary [NX 7550 4540] 

where the sequence comprises (base upwards) of about 

210 m of conglomeratic sandstones, siltstones, ‘marls’ 

and shales with isolated dolostone nodules; 120 m of 

sandstones (sometimes conglomeratic), siltstone and shale; 

and more than 40 m of coarse conglomerates, interbedded 

with conglomeratic sandstones and a few thin red ‘marls’ 

(deegan, 1973; see also lintern and Floyd, 2000, p. 83–85). 


The base is unconformable on turbidites of the silurian 

Raeberry Castle Formation, Riccarton Group. 

The top of the member is faulted against the coarse conglomeratic 

red bed facies of the orroland member (Figure 

10, Column 1). 

Thickness 

About 370 m 


Coastal outcrop between white port [NX 7234 4336] and 

port mary [NX 7550 4540], south-west scotland (solway 

Firth). 

Age 

Tournaisian. 

6.3.6.3 orrolanD MeMBer (orr) 

Name 

previously known as the orroland limestone Beds by Craig 

and Nairn (1956), the orroland Group by deegan (1973), 

and the orroland Formation by lintern and Floyd (2000). 

The status is here changed to a member. 

Lithology 

Conglomerates, conglomeratic sandstones, sandstones, red 

siltstones, ‘marls’ and pedogenic dolostones (‘cornstones’). 

Stratotype 

The type section is the coastal section from port mary 

to Castle muir [NX 7445 4537 to 7980 4720] where the 

83 

sequence comprises (base upwards) of about 90 m of 

conglomerates and sandstones; 18 m of conglomeratic 

sandstones, siltstones, ‘marls’ and dolostones; 25 m of 

conglomeratic sandstones, and silty and sandy ‘marls’ with 

dolostone nodules; about 10 m of calcareous sandstones, 

mudstones, ‘marls’ and impure marine limestones; about 

9 m of burrowed marine sandstone; 28 m of conglomeratic 

sandstones and ‘marls’ with dolostone nodules; and 

90–100 m of conglomeratic sandstones and sandstones 

(deegan, 1973; see also lintern and Floyd, 2000, p. 85). 


The base of the member is faulted against the sandstones 

and conglomerates of the wall Hill member (Figure 10, 

Column 1). 

The top of the member is faulted against the conglomeratic 

sandstone and thin interbeds of calcareous mudstone 

and siltstone of the Rascarrel member (Fell sandstone 

Formation). 

Thickness 

About 280 m. 


Coastal section from port mary [NX 7445 4537] to Castle 

muir [NX 7980 4720], south-west scotland (solway Firth). 

Age 

Chadian. 

6.4 RAVENSTONEDALE GROUP (RVS) 

The Ravenstonedale Group, named after the Ravenstonedale 

area of Cumbria, is of continental and peritidal facies. it 

comprises a typically thin succession, with geographically 

isolated outcrops present across parts of Cumbria. 

lithologically, the group includes green to green-grey 

and/or variably reddened pebble conglomerate (locally 

calcite cemented), lithic sandstone, sandstone and mudstone. 

evaporitic deposits have been recorded in boreholes. 

pedogenic carbonates occur within the sandstones, 

though they are less common than within the Kinnesswood 

Formation of the inverclyde Group. Conglomerates have 

a local provenance, and basaltic lava flows occur locally 

within the alluvial fan facies. The most diverse lithological 

development is in the western part of the stainmore Trough 

and northern part of the Askrigg Block. 

within the Stainmore Trough the group comprises the 

pinskey Gill, marsett, Cockermouth volcanic, stone Gill 

limestone and shap village limestone formations (the last 

mentioned also occurring on the Alston Block and in east 

Cumbria). 

on the Askrigg Block the group comprises the Raydale 

dolostone, marsett and penny Farm Gill formations. 

in north, south and west Cumbria the group comprises 

the marsett Formation. in the Kendal area it is here suggested 

that what is presently assigned to the lower part of a 

local equivalent of the martin limestone Formation, Great 

scar limestone Group of open marine, platform and ramp 

carbonates facies, is more typical of the Ravenstonedale 

Group (see section 6.6.19). 

on the Isle of Man, the langness Conglomerate 

Formation (formerly the ‘Basement Conglomerate’) is tentatively 

referred to the Ravenstonedale Group. 

The on-lapping succession of the group was deposited 

within an epicontinental basin as alluvial fan, fluviodeltaic, 

marginal marine and peritidal deposits (Holliday et al., 1979). 



deposition on the Askrigg Block occurred following early 

visean sea-level rise, with the succession located marginal 

to the more open marine conditions present in the stainmore 

Trough at the time. outside of the stainmore Trough and 

northern part of the Askrigg Block the group is dominated by 

alluvial fan subfacies deposited within linked basins. 

The group rests unconformably upon rocks ranging from 

ordovician to devonian in age, including the wensleydale 

Granite beneath the Askrigg Block at Raydale. limestone 

formations at the base of the Great scar limestone Group 

(open marine, platform and ramp carbonates facies) define 

the top of the Ravenstonedale Group – though locally, a 

nodular dolostone bed with rhizoliths, indicative of emergence, 

marks the top of the group on the Askrigg Block 

(Burgess, 1986). 

occurring across Cumbria and north yorkshire, the 

Ravenstonedale Group is thickest in the western part of 

the stainmore Trough (about 380 m) and northern part of 

the Askrigg Block (about 150 m). in south Cumbria, in the 

duddon estuary, it attains a maximum thickness of 240 m 

thinning appreciably towards the south and east. in north 

and east Cumbria the group is typically less than 35 m 

thick. within the stainmore Trough it is Tournaisian in age. 

whilst on the northern margin of the Askrigg Block it is 

Chadian to early Holkerian. 

STAINMORE TROUGH (Figure 9, Column 16): 

6.4.1 Pinskey Gill Formation (PNKG) 

Name 

derived from pinskey Gill, by Newbiggin on lune, 

Cumbria. The formation was originally named the pinskey 

Gill Beds by Garwood (1913, p. 496). 

Lithology 

The pinskey Gill Formation comprises grey, vuggy, 

dolomitic limestone and dolostone interbedded with grey to 

dark grey calcareous mudstone and thin-bedded, calcareous, 

silty sandstone. 


The strata were deposited in a peritidal marine and fluvial 

environment. 

Stratotype 

The type section is in pinskey Gill [Ny 698 040] where 

the formation is about 20 m thick and comprises beds of 

sandstone, calcareous mudstone with sporadic pebbles, 

sandy shale, interbedded mudstone and shale, and dolomite, 

(see Garwood, 1913, pp. 496– 499). 


The formation rests unconformably upon a smooth planation 

surface cut into lower palaeozoic strata. Conglomerate 

beds of the marsett Formation overlie it unconformably 


Thickness 

up to 50 m. 


The formation is found only at Ravenstonedale in the 

stainmore Trough. 


miospores including Schopfites claviger and S. delicatus 

of the Cm and possibly pC zones (Johnson and marshall, 



84 

1971; Holliday et al., 1979) and conodonts dominated 

by Bispathodus aculeatus aculeatus, B. stabilis and 

Clydagnathus unicornis of the Pseudopolygnathus 

multistriatus Zone (varker and Higgins, 1979; varker and 

sevastopulo, 1985) indicate a Tournaisian (mid Courceyan) 

age for the formation (Table 2). 

6.4.2 Marsett Formation (MASA) 

Name 

The formation, locally referred to as the ‘basement beds’, 

feldspathic conglomerate, quartz conglomerate, greywacke 

sandstone, etc., in previous work (see for example Garwood, 

1913; Rose and dunham, 1977; mitchell, 1978; pattison, 

1990) is named after the hamlet of marsett in Raydale. 

Lithology 

The marsett Formation comprises laterally variable beds 

of conglomerate, lithic sandstone and mudstone. The 

sandstone beds are generally cross-bedded and may be in 

shades of brown, red, grey, green or buff. over much of the 

stainmore Trough, the marsett Formation comprises red 

sandstone, green shale and conglomerate. on the Askrigg 

Block the formation consists of reddish brown and greenish 

grey sandstone and conglomerate with rare dolostone 

beds. in north Cumbria, basaltic lavas of the Cockermouth 

volcanic Formation occur within the alluvial fan facies of 



in most instances the beds are fluvial in origin, though 

reworking in shallow marginal marine conditions may have 

occurred locally. 

Stratotype 

The type section is from about 406 to 463 m depth in the BGs 

Raydale Borehole (BGs Registration Number sd98sw/1) 

[sd 9026 8474] on the Askrigg Block. localities in the 

Appleby district include shap Abbey [Ny 5482 1533] 

where about 9 m of shaly sandstone and conglomerate 

occur in a cliff on the River lowther (see Garwood, 1913), 

and Holghyll [Ny 4290 2730] where a thick succession is 

accessible in the ravine (see mcCormac, 2001, p. 12). 


The marsett Formation rests unconformably upon the 

limestones, mudstones and sandstones of the pinskey Gill 

Formation in the stainmore Trough (Figure 9, Column 16) 

and on the siltstones and sandstones with thin-bedded and 

nodular dolostones of the Raydale dolostone Formation 

on the Askrigg Block (Figure 9, Column 17; Figure 15, 

Column 3). in the Furness area the formation is underlain 

unconformably by unspecified lower palaeozoic strata 

(see section 6.4.2.1). The formation is contiguous with 

the overlying marine Tournaisian/visean succession. This 

comprises in the stainmore Trough and on the Askrigg Block 

the limestones, sandstones and mudstones of the stone Gill 

limestone and penny Farm Gill formations respectively. 

North of the River lowther in westmorland the formation 

is overlain by the dolostones of the shap village limestone 

Formation (the base of which is marked by beds with algal 

mats and nodules) (Figure 14, Column 3). Near orton, 

east of shap, in a gully section next to the m6 motorway 

[Ny 600 075] black marine mudstone beds of the marsett 

Formation lie beneath calcareous limestone and siltstone 

beds of the stone Gill limestone Formation (see pattison, 

1990, p. 9; day, 1992, p. 15; mcCormac, 2001, p. 12) 

(Figure 9, Column 16). on the Alston Block and in north and

18 

INGLETON 

COALFIELD 

15 

16 

ALSTON STAINMORE 

13 

NORTH, EAST AND 

WEST CUMBRIA 

PENNINE MIDDLE 

COAL MEASURES 

FORMATION 

WARWICKSHIRE 

GROUP 

17 

ASKRIGG 

VDMB 

M 

PENNINE LOWER 


M 

PENNINE COAL 

MEASURES 

GROUP 

WHITEHAVEN 

SANDSTONE FM 

PENNINE LOWER 


SBMB 

14 

SOUTH CUMBRIA 

(Furness) 

CAMB 

PENNINE UPPER 


M 

PENNINE UPPER 

COAL MEASURES 

FORMATION 

G1A1 

L 

M 

MARSDEN 

HEBDEN FM FORMATION 

M ISMB 

M 



ROSSENDALE 

FORMATION 

VDMB 

M 

PENNINE COAL 



COAL MEASURES 

FORMATION 

STAINMORE 

FORMATION 

SBMB 

PENDLETON 

FORMATION 

M 

PENNINE LOWER 


VDMB? 

BOWLAND SHALE 

FORMATION 

M 

ALSTON 

FORMATION 

STAINMORE 

FORMATION 

PENNINE LOWER 

COAL MEASURES 

FORMATION 

PENNINE COAL MEASURES GOUP 

PENNINE LOWER 

COAL MEASURES 

FORMATION 

PENNINE COAL 

MEASURES 

SBMB GROUP 

PENNINE COAL 

MEASURES GP 

E2AI L 

MULLSTONE GRIT 

GROUP 

STAINMORE 

FORMATION 

SAMLESBURY FM 

SILSDEN FM 

M 

PENDLETON FM 

STAINMORE FM 


MILLSTONE 

GRIT GP 

GL 

GL 


CRAVEN 

GROUP 

GL 

E1A1 

GL 

YOREDALE 

GROUP 

ALSTON 

FORMATION 

ALSTON 

FORMATION 

GVB 

SBMB? 

L 

YOREDALE 

GROUP 

ALSTON 

FORMATION 

YOREDALE 

GROUP 

URSWICK LIMESTONE 

FORMATION 

KNIPE SCAR 

LIMESTONE FM 

ALSTON 

FORMATION 

WINTERTARN SANDSTONE MEMBER 

(TYNE LIMESTONE FORMATION) 

DANNY BRIDGE 

LIMESTONE FM 

PARK LIMESTONE 

FORMATION 

ESKETT LIMESTONE 

FORMATION 

FRIZINGTON 

LIMESTONE FM 

MARTIN LIMESTONE FM 

GREAT SCAR 

LIMESTONE 

GROUP 

ASHFELL 

LIMESTONE FM 

WINTERTARN 

SANDSTONE 

MEMBER 

(TYNE LIMESTONE 

FORMATION) 

GARSDALE LIMESTONE 

FORMATION 

ASHFELL SANDSTONE 

FORMATION 

FAWESWOOD 

LIMESTONE FM 

GREAT SCAR 

LIMESTONE GP 

GREAT SCAR 

LIMESTONE GP 

RED HILL 

LIMESTONE 

FORMATION 

DALTON 

FORMATION 

GREAT SCAR 

LIMESTONE GROUP 

MARSETT 

FORMATION 

v v v 

TOM CROFT 

LIMESTONE FM 

PENNY FARM GILL FM 

BROWNBER 

FORMATION 

SCANDAL BECK 

LIMESTONE FM 

RNL 

COCKERMOUTH 

VOLCANIC 

FORMATION 


GROUP 

MARSETT FORMATION 

RAYDALE DOLOSTONE 

FORMATION 

MELMERBY SCAR 

LIMESTONE FM 

MARSETT FM 

GREAT SCAR 

LIMESTONE 

GROUP 

MARTIN LIMESTONE 

FORMATION 

MARSETT 

FORMATION 


GROUP 

PGL 

POTTS BECK 

LIMESTONE 

FORMATION 

BZB 

ASHFELL 

SANDSTONE 

FORMATION 

COUPLAND SYKE 

LIMESTONE 

MEMBER 

PARK HILL 

LIMESTONE MEMBER 

COLDBECK 

LIMESTONE 

FORMATION 

STONE GILL 

LIMESTONE FM 

MARSETT FM 

PINKEY GILL FM 


GROUP 


GROUP 


GROUP 

SCALE 

200 

85 

DUDDON 

CONGLOMERATE 

MEMBER 

metres 

0 

LOCALITIES 

N 

15 

13 16 

17 

18 

14 

98001784 

Figure 9 Generalised vertical sections and correlation for Carboniferous strata in Cumbria, Alston, stainmore, Askrigg and the ingleton Coalfield. Based on Ford (1954), 

iGs (1973), George et al. (1976), mitchell (1978), Ramsbotton (1978), Ramsbottom et al. (1978), dunham and wilson (1985), Arthurton et al. (1988), pattison (1990) and 

millward et al. (2003). The profiled location of the numbered sections is given in the inset map. see Appendices 1 and 2 for the names of the lithostratigraphical units shown 

by BGs lexicon of Named Rock units computer codes. m marine band; l Lingula band. v indicates named volcanic rock units; blue colour indicates named limestone 

beds. wavy lines indicate unconformity surfaces. 



west Cumbria the conglomerates of the marsett Formation 

are, respectively, unconformably and disconformably overlain 

by the carbonates of the melmerby scar limestone and 

Frizington limestone formations, Great scar limestone 

Group (Figure 9, Column 15; Figure 14, Columns 1, 2), 

though at the northern margin of the lake district the top 

of the marsett Formation conformably underlies the basalt 

lavas of the Cockermouth volcanic Formation (Figure 14, 

Column 2). in the Furness area the formation passes conformably 

up to grey, red and green marine mudstone and 

limestone of the martin limestone Formation (Figure 9, 

Column 14) (see sections 6.4.2.1 and 6.6.19). 

Thickness 

in most areas the formation is thin. in the Appleby district 

it is 2–20 m thick. in north and east Cumbria it is typically 

less than 35 m thick. on the Askrigg Block it is 60 m thick. 

However, on the northern margin of the stainmore Trough, at 

Roman Fell [Ny 760 200], beds up to 200 m thick are present. 

The formation is up to 240 m thick in the Furness area. 


present in north, east and west and south Cumbria and 

throughout north yorkshire, including the stainmore Trough 

and Askrigg Block. in the Kendal area it is suggested that 

what is presently assigned to the lower part of a local 

equivalent of the martin limestone Formation, Great scar 

limestone Group of open marine, platform and ramp 

carbonates facies, is more typical of the Ravenstonedale 

Group (see section 6.6.19). 


miospore assemblages from a number of sites including 

Cockermouth, Ravenstonedale and Furness (mitchell, 1978; 

Holliday et al., 1979; Rose and dunham, 1977) all indicate a 

Cm Zone, Tournaisian age for the formation. However, the 

beds pass upwards in unbroken succession into limestone, 

which may be as young as Holkerian. Biostratigraphy of 

the Raydale Borehole (see above) suggests a possible late 

Chadian age for the formation at this locality on the Askrigg 

Block (see dunham and wilson, 1985). The full age range 

of the formation is therefore currently undetermined. 


see also Appendix 1. The marsett Formation includes one 

formal member: 

6.4.2.1 DuDDon CongloMeraTe MeMBer (DuCo) 

Name 

see Johnson et al. (2001); Rose and dunham (1977). 

Lithology 

Conglomerate, sandstone and mudstone, mainly red-brown 

with pale green and mottled layers, with traces of evaporite. 

large clasts (pebbles up to 15 cm) are well rounded, 

commonly with ferruginous skins. Clast lithologies all 

occur locally and include Borrowdale volcanic Group 

andesite, tuff and rhyolite, silurian ‘grit’ and ‘greywacke’ 

and eskdale Granite and ennerdale Granophyre. 

Stratotype 

The type section is a borehole (BGs Registration Number 

sd27Nw/323) [sd 2113 7991] between 88.52 and 255.50 

m depth (see Rose and dunham, 1977). 


The base is unconformable on the top of the lower 

palaeozoic basement (Figure 9, Column 14). 



86 

The top of the member occurs at upward change from 

conglomerate beds to grey, red and green marine mudstone 

and limestone with subordinate thin conglomerate beds 

of the martin limestone Formation. The junction may be 

sharply gradational or possibly an onlap surface. 

Thickness 

maximum recorded 240 m in dunnerholme (Rose and 

dunham, 1977). 


Furness, Cumbria confined to the area of the duddon 

estuary. 

Age 

Courceyan. 

6.4.3 Cockermouth Volcanic Formation (CKML) 

Name 

originally named the Cockermouth lavas (eastwood, 

1928). see also millward in stephenson et al. (2003); 

macdonald and walker (1985). 

Lithology 

Basalt, olivine-phyric and andesite, tholeiitic. up to four 

sheets of massive to intensely amygdaloidal and scoriaceous 

rock, dark blue-grey to grey. interpreted to be lavas. No 

intercalated pyroclastic or sedimentary rocks are present. 

Stratotype 

The partial type section is Gill Beck, immediately south 

of Blindcrake, about 4.5 km north-east of Cockermouth, 

Cumbria [Ny 149 341 to 149 344] where a sequence of at 

least four tholeiitic olivine-phyric basalt lavas about 67 m 

thick can be seen, though the base and top of the succession 

is not exposed (see millward in stephenson et al., 2003, 

pp. 116–120). A reference section is Bothel Craggs Quarry, 

on the west side of the A591 road, about 1.5 km south-southeast 

of Bothel, Cumbria [Ny 186 371] where apparently 

one, sparsely amygdaloidal tholeiitic andesite about 4 m 

thick is seen, though the base and top of the succession 

are not exposed (see millward in stephenson et al., 2003, 

pp. 120–122). 


in north Cumbria the base is conformable on the 

conglomerates and sandstones of the marsett Formation, 

and the top lies beneath bedded mudstone, limestone 

and sandstone at the base of the Great scar limestone 

Group (specifically beneath a conglomerate developed 

locally at the base of the Frizington limestone Formation) 


Thickness 

some 105 m in the Cockermouth area; 67 m thick in the 

type section. 


Northern margin of the lake district lower palaeozoic 

massif, from just west of Cockermouth to Bothel. intrusions 

of dolerite and deposits of lapilli-tuff on little mell Fell, 

in the Appleby district, may include intrusive equivalents 

to the Cockermouth volcanic Formation (macdonald and 

walker, 1985). 

Age 

Courceyan.


1 

N 

1 

ORROLAND AND 

WALL HILL 


SCALE 

metres 

150 

0 

ORROLAND 

MEMBER 

WALL HILL 

MEMBER 

2 

SOLWAY FIRTH 

INVERCLYDE 

LOCALITIES 

YOREDALE 

GROUP 

TYNE LIMESTONE 

FORMATION 

BORDER GROUP 

2 

KIRKBEAN 

FELL SANDSTONE 

FORMATION 

LYNE 

FM 

3 

ARBIGLAND 

LIMESTONE 

MEMBER 

POWILLIMOUNT 

SANDSTONE 

MEMBER 

GILLFOOT 

SANDSTONE 

MEMBER 

98001785 

THSD 

SOUTHERNESS 

SYGL 


GROUP KIRKBEAN 

CEMENTSTONE 

MEMBER 

v v 

BIRRENSWARK VOLCANIC 

BALLAGAN 

FORMATION 

FORMATION 

KINNESSWOOD 

FORMATION 

87 

PENNINE LOWER 

COAL MEASURES 

FORMATION 

PENNINE COAL MEASURES GROUP 

YORESDALE GROUP 

INVERCLYDE GROUP BORDER GROUP 

3 

LANGHOLM 

PENNINE UPPER COAL 


PENNINE 

MIDDLE COAL 

MEASURES FM 

STAINMORE 

FORMATION 

ALSTON 

FORMATION 

TYNE LIMESTONE FORMATION 


FORMATION 

LYNE 

FORMATION 

BALLAGAN 

FORMATION 

v 

v 

v 

M 

M 

M 

M 

M 

M 

M 

M 

M 

M 

M 

M 

M 

M 

M 

M 

M 

GV 

KHB 

LARS 

M 

v 

BIRRENSWARK 

VOLCANIC 

FORMATION 

v 

KINNESSWOOD 

FORMATION 

CAMB (RSMB) 

SFMB (RTMB) 

EMMB(VMB) 

AGMB(SNMB) 

SOMB (KMMB) 

HTMB(SHMB) 

VDMB (QMB) 

UFTL 

NWL 

THL 

AOB 

UOL 

LOL 

BPLS 

FOUR FATHOM 


TMBL EELWELL 

BRDL 

PNLS 

CALS 

AKB 

KTLS 

DIB 

BUBE 

HGLS 

SCOT 

Figure 10 solway Basin. Representative sections for Carboniferous strata at orroland and wall Hill, 

Kirkbean and langholm. Based on lumsden et al. (1967) and lintern and Floyd (2000). The profiled location 

of the numbered sections is given in the inset map. see Appendices 1 and 2 for the names of the 

lithostratigraphical units shown by BGs lexicon of Named Rock units computer codes. m marine band; 

v indicates named volcanic rock units; blue colour indicates named limestone beds; green colour indicates 

significant developments of named sandstone units. wavy lines indicate unconformity surfaces. 

HNB 

CEBS 

GREAT 

LIMESTONE 

MEMBER 

LIMESTONE 

MEMBER 



6.4.4 Stone Gill Limestone Formation (STE) 

Name 

The name comes from that proposed by Garwood (1907) 

and defined in the type section at stone Gill by Ramsbottom 

(1973). 

Lithology 

The stone Gill limestone Formation comprises grey, 

porcellanous limestone and thin dolostone, with beds of 

argillaceous limestone, sandstone and mudstone common 

above the base. Calcretes, desiccation structures and 

pseudomorphs after evaporites are also present. 


The presence of calcretes, desiccation structures and 

evaporite pseudomorphs (Holliday et al., 1979) indicate 

deposition in a quiet, nearshore to peritidal restricted marine 

environment. 

Stratotype 

The type section is in stone Gill [Ny 718 040] as defined 

by Ramsbottom (1973). A locality in the Appleby district is 

shap Abbey [Ny 5478 1550] where about 18 m of dolostone 

and ‘magnesian’ limestone is exposed in a cliff on the 

east bank of the River lowther (see Garwood, 1913). see 

also the wyegarth Gill No. 1 Borehole (BGs Registration 

Number Ny70sw/1) [Ny 7201 0354] and the gully section 

next to the m6 motorway [Ny 600 075] mentioned below 

with regard to the lower boundary of the formation. 


The base of the formation is conformable. defined at a 

depth of 49.73 m in the wyegarth Gill No. 1 Borehole 

(see above) where there is a gradational change in rock 

type from the underlying sandstones and siltstones of the 

marsett Formation to a sequence of limestones, sandstones 

and mudstones of the stone Gill limestone Formation. 

However, the base can be precisely located in a gully 

section next to the m6 motorway [Ny 600 075], where 

calcareous siltstone and limestone beds rest on black marine 

mudstone beds marking the top of the marsett Formation 

(see pattison, 1990, p. 9; day, 1992, p. 15; mcCormac, 

2001, p. 12; Figure 9, Column 16). 

The formation is conformably overlain by the Coldbeck 

limestone Formation of the Great scar limestone Group 

south of the Anne’s well Fault (Figure 9, Column 16), and 

by the shap village limestone Formation, Ravenstonedale 

Group, north of it. 

Thickness 

up to 100 m thick in the Ravenstonedale area. 20–40 m 

thick in the Appleby district. 


stainmore Trough. in the Kendal area, strata presently 

assigned to the lower part of a local equivalent of the 

martin limestone Formation, Great scar limestone Group 

of open marine, platform and ramp carbonates facies, 

is suggested to be more typical of the Ravenstonedale 

Group. This appears to be further supported by the 

striking similarity noted in field characteristics between 

this succession and the stone Gill limestone Formation 

(see section 6.6.19). 


The formation has a restricted marine biota of algae 

(including Solenopora sp.), foraminifers (including Brunsia 



88 

sp. and Dainella sp.), Syringopora sp., ‘Camarotoechia’ 

proava, Cleiothyridina glabistria, vermetid gastropods, 

and ostracods. it was considered to be early Chadian 

(Tournaisian) in age by Holliday et al. (1979). However, 

the upper part has a pu Zone miospore assemblage, and 

‘Camarotoechia’ proava and Cleiothyridina glabistria 

are late Chadian chronozonal brachiopods (see Garwood, 

1913). The succession apparently includes the early–late 

Chadian (Tournaisian–visean) boundary but its position is 

uncertain. it may exist near the top of the formation. 

6.4.5 Shap Village Limestone Formation (SHVI) 

Name 

The name is derived from the village of shap, Cumbria. The 

name shap village limestone Formation was introduced by 

mcCormac (2001) and the unit is equivalent to the shap 

limestone of dakyns et al. (1897; see millward et al. 2003, 

p. 13). 

Lithology 

The shap village limestone Formation is composed, in 

its lower part, of well-bedded dolostone with interbeds 

of siltstone and calcareous sandstone. in its middle part 

it consists of cross-bedded, dark grey, sandy packstone/ 

grainstone with the coral genus Dorlodotia. in its upper part 

it comprises finely cross-laminated oolites, thick-bedded 

calcareous, rippled sandstone, pebbly sandstone, and crossbedded 

calcarenite. 


The depositional environments include fluvial and marginal 

marine. 

Stratotype 

The partial type section is in Force Beck [Ny 5684 1384 

to 5772 1354] where the basal algal beds are overlain by 

a mudstone seatearth, dolostone (20–40 m thick) with 

thin interbeds of siltstone or fine-grained sandstone, of 

packstone/grainstone (also 20–40 m thick and with thin 

interbeds of siltstone or fine-grained sandstone), oolitic 

limestone, and a mixed succession of calcareous sandstone, 

pebbly sandstone, and oolites. The section is incomplete 

due to faulting (see mcCormac, 2001, pp. 12–13). Another 

locality in the Appleby district is loudon Hill [Ny 4650 

2725], dacre, where workings in the upper sandstones can 

be seen (see mcCormac, 2001, p. 13). 


Beds with algal mats and nodules mark the base of the shap 

village limestone Formation. North of Anne’s well Fault 

in the shap area the formation overlies the limestones with 

sandstones and mudstones of the stone Gill limestone 

Formation, and north of the River lowther in westmorland 

it overlies the sandstone and conglomerate dominated 

marsett Formation. 

The top of the shap village limestone Formation is 

marked by distinctive pebble beds and is overlain conformably 

by the Ashfell sandstone Formation (Great scar 

limestone Group) (Figure 14, Column 3). 

Thickness 

The formation is 40–120 m thick, and 70–100 m thick in 

the Appleby district. 


The shap–penrith area, east Cumbria (mcCormac, 2001), 

extended to include equivalent rocks assigned to the

‘Ravenstonedale limestone’ in the Alston and Brough 

areas (Arthurton and wadge, 1981; Burgess and Holliday, 

1979). 


The coral genus Dorlodotia, described from several 

localities in the shap and Askham area (dean, 2001), 

indicates a late Chadian age for the bulk of the formation. 

Garwood (1913) described a coral/brachiopod fauna 

typical of his Camarophoria isoryncha subzone at the 

top of the succession at shap. in the correlation of 

George et al. (1976), this would place the upper part of 

the formation in the Arundian. However, more recently, 

Riley (1993) has argued that all the rocks found at this 

level in the Ravenstonedale area are Chadian in age, and 

this cannot be refuted in the apparent absence of of data 

concerning the presence of archaediscid foraminifers, 

the first entry of primitive forms defining the base of the 

Arundian. 

ASKRIGG BLOCK (Figure 9, Column 17): 

6.4.6 Raydale Dolostone Formation (RDO) 

Name 

The name is derived from the Raydale dolomite Formation 

as described in the Raydale Borehole (see below). see 

dunham and wilson (1985, p. 26, fig. 5, and references 

therein). 

Lithology 

The Raydale dolostone Formation comprises thinly 

bedded and nodular dolostones (‘cementstones’) 

interbedded with siltstone and sandstone. The strata are 

similar to those present in the Ballagan Formation of 

the midland valley of scotland and Northumberland 

Trough. 


marginal marine 

Stratotype 

The formation occurs in the BGs Raydale Borehole (BGs 

Registration Number sd98sw/1) [sd 9026 8474] between 

about 463 and 495 m depth where it comprises thinly 

bedded and nodular dolostones with much interbedded 

siltstone and fine-grained sandstone (dunham and wilson, 

1985, p. 26). 


The formation occurs immediately above the wensleydale 

Granite, which was reached in the Raydale Borehole (see 

above) at 495.05 m depth. 

The top of the formation occurs at the base of the 

conglomeratic marsett Formation (Figure 9, Column 17; 

Figure 15, Column 3). 

Thickness 

About 30 m. 


Askrigg Block. 


miospores indicate a Chadian (post-Tournaisian) age for 

the formation (owens, pers. comm. reported in waters et 

al. 2007). 

89 

6.4.7 Marsett Formation (MASA) 


6.4.8 Penny Farm Gill Formation (PFD) 

Name 

The name is derived from penny Farm Gill, Askrigg Block. 

The original name ‘penny Farm Gill dolomite Formation’ 

was proposed by Burgess (1986, p. 6). 

Lithology 

The penny Farm Gill Formation comprises interbedded 

limestone, dolostone, sandstone and siltstone, commonly 

rhythmically bedded. 


The strata were deposited within a shallow marine, intertidal 

and supratidal environment, marginal to the more open 

marine conditions in the stainmore Trough at the time. 

Stratotype 

partial type sections include the lowest 17 m of the formation 

seen in Nor Gill [sd 698 933] in a sequence that comprises 

mainly sandstones, silty limestones and siltstones; and the 

succeeding 35 m of beds, which are well seen in the inlier at 

penny Farm Gill [sd 698 932], where the sequence comprises 

sandy and micritic dolostones, siltstone with dolostone beds 

(not exposed, but suggested by debris), and sandy limestones 

with interbedded dolostones (Burgess, 1986, pp. 6–7; see 

also dunham and wilson, 1985, p. 26). The formation also 

occurs in the Raydale Borehole (BGs Registration Number 

sd98sw/1) [sd 9026 8474] from about 350 to 406 m depth 

(see dunham and wilson, 1985, and references therein). 


The formation overlies contiguously the conglomeratic 

marsett Formation. 

The top of the penny Farm Gill Formation is marked 

locally by a nodular dolostone bed with rhizoliths that is 

indicative of emergence (Burgess, 1986). The biosparites of 

the Tom Croft limestone Formation (Great scar limestone 

Group) disconformably overlie the formation (Figure 9, 

Column 17; Figure 15, Column 3). 

Thickness 

According to dunham and wilson (1985) the formation is 

50.6 m thick in the penny Farm Gill inlier, and about 56 m 

thick in the Raydale Borehole (see above). 

Distriution and regional correlation 



The formation has a limited fauna of bivalves, gastropods, 

the brachiopod Rhynchonella fawcettensis, and ostracods. 

However, a miospore assemblage from the formation has 

been assigned to the (Chadian to Arundian) pu Zone, although 

the presence of Knoxisporites stephanephorus suggests an 

Arundian to early Holkerian age Ts Zone (Burgess, 1986). 

ISLE OF MAN (Figure 8, Column 8): 

6.4.9 Langness Conglomerate Formation (LNCO) 

Name 

The name is derived from langness, south isle of man, and 

was given by dickson et al. (1987). 



Lithology 

The formation comprises reddish brown, generally poorly 

sorted, typically clast-supported conglomerate with 

subordinate interbedded sandstone. sedimentary structures 

include crude stratification and rare cross-bedding. see 

Chadwick et al. (2001). 


The formation is an alluvial fan deposit, transported by 

debris flow and streamflow processes. 

Stratotype 

A partial type section includes foreshore exposures along 

the langness peninsula [sC 2819 6604 to 2854 6661] where 

an estimated 30 m of coarse clastic sedimentary rocks are 

present (see dickson et al., 1987, p. 205). 


The formation is unconformable on the underlying, steeperdipping, 

ordovician lonan Formation (see Chadwick et al., 

2001). 

The limestones of the Turkeyland member, derbyhaven 

Formation, Great scar limestone Group (Figure 8, 

Column 8) overlie the apparently partly reworked sandstone 

top to the langness Conglomerate Formation. 

Thickness 

The formation is about 30 m thick. 


The formation occurs in the south isle of man. 

Age 

?devonian to Courceyan (Chadwick et al., 2001, p. 59) 

6.5 BORDER GROUP (BDR) 

The Border Group (lumsden et al. 1967; day, 1970) 

consists of two sedimentary formations corresponding 

to some extent to the geographically extended, former 

lower and middle Border groups of day (1970; see also 

waters et al., 2007). The lower, the lyne Formation (which 

equates with the ‘Cementstones’ of older terminology in 

Northumberland) comprises strata of heterolithic clastic 

and nonmarine carbonate facies. The Fell sandstone 

Formation, of fluviodeltaic (‘Millstone Grit’) facies, 

diachronously overlies the lyne Formation. Thin olivine 

basalt lavas occur as the Kershopefoot basalts (williamson 

in stephenson et al., 2003). 

The base of the group is conformable where the interbedded 

sandstones, limestones, anhydrites, rootlet beds and thin 

coals of the Ballagan Formation (inverclyde Group) pass 

upward into the cyclical sequences of sandstone, mudstone 

and thin limestone of the lyne Formation. This is the presumption 

at Bewcastle and Kirkbean, and it has been proved 

in a borehole at Annandale. The base is also conformable at 

Brampton where the Ballagan Formation passes upwards into 

the sandstone-dominated Fell sandstone Formation. However, 

in the north-east part of the Northumberland Trough the same 

boundary is unconformable; and within the central part of the 

trough, the base of the group has not been proved. The base 

of the yoredale Group (mixed shelf carbonate and deltaic 

(‘Yoredale’) facies) defines the top of the Border Group. 

The Border Group is restricted in geographical extent 

to the Northumberland Trough and solway Basin, and is 

greater than 1350 m thick in the central part of the former. 

it is late Tournaisian to Holkerian in age. 



90 

6.5.1 Lyne Formation (LYNE) 

Name 

The lyne Formation is synonymous with the Cementstone 

series of the Bewcastle district as defined by Garwood 

(1913). it equates with the lower Border Group of lumsden 

et al. (1967) and day (1970), and is named after the River 

white lyne at Bewcastle (day, 1970). see also lintern and 

Floyd (2000). 

Lithology 

in the Northumberland Trough, the lyne Formation 

comprises cyclical sequences of fine-grained subarkosic 

sandstone, siltstone, mudstone, and thin limestone in which 

thin oolitic pellet beds are characteristic components. in the 

solway Basin, in the easton 1 borehole (BGs Registration 

Number Ny47sw/15) [Ny 44124 71694] the formation is 

represented by the easton Anhydrite member, of grey or 

white anhydrite interbedded with limestone, shale, siltstone 

and sandstone. 


The lyne Formation limestones are typically peritidal, 

with the first incoming of marine limestones occurring 

later towards the north-east of the Northumberland Trough, 

north-east of Bewcastle. The sandstones were deposited 

from lobate deltas that migrated periodically along the 

basin axis from north-east to south-west (leeder, 1974). 

in the solway Basin, the easton Anhydrite member is 

predominantly of shallow water origin. The sediments 

were deposited in a rapidly subsiding basin, with restricted 

marine circulation, in which sedimentation and rapid 

burial is inferred to have kept pace with subsidence. most 

of the anhydrite is likely to have had a subaqueous rather 

than a sabkha origin, the purer and thicker beds probably 

precipitating as gypsum in regionally extensive salinas. 

Stratotype 

Type sections of the constituent members include for the 

easton Anhydrite member, the easton 1 borehole (see 

above) from 1054 to 2260 m depth (this is a partial type 

section since the base of the member is not proved); for 

the southerness limestone member, the shore section 

at southerness [NX 9690 5420 to 9740 5420]; for the 

lynebank member, ellery sike [Ny 5433 7584] to 

Nixontown [Ny 5482 7550] on the River white lyne; 

for the Cambeck member, the River white lyne [Ny 

5116 7300 to 5109 7322] at Bewcastle; for the main Algal 

member, Birky Cleuch [Ny 5885 7540 to 5932 7538], 

Kirk Beck, Bewcastle; and for the Bewcastle member, 

Ashy Cleuch [Ny 5648 7698 to 5808 7665] upstream from 

stockastead Quarry. 


The formation in the central part of the Northumberland 

Trough passes northward, by lateral facies change, into strata 

of the Ballagan Formation, inverclyde Group (Figure 8, 

Column 11). in Annandale, the Hoddom No. 2 Borehole 

(BGs Registration Number Ny17se/3) [Ny 1641 7285] 

showed the lyne Formation conformably overlying the 

Ballagan Formation at 139.84 m depth. The base of the lyne 

Formation is not seen at Bewcastle (Figure 11, Column 2) 

or Kirkbean (Figure 10, Column 2) but it is presumed to rest 

conformably on the Ballagan Formation in these places. The 

base of the easton Anhydrite member is not seen, but seismic 

interpretation indicates the presence of ‘several thousands of 

feet’ of conformable strata below the succession in some 

parts of the solway Basin (see ward, 1997, p. 283).

The upper boundary of the formation is locally unconformable 

and diachronous with the Fell sandstone Formation 

in the central parts of the Northumberland Trough. At 

Bewcastle, the base of the latter is locally defined as the 

base of the whitberry Band (wBB) (Figure 11, Column 2). 

The top of the easton Anhydrite member is taken where 

numerous beds of anhydrite interbedded with limestones, 

shales, siltstones and sandstones give way to strata with 

variously algal, oolitic, peloidal, shelly, crinoidal and 

serpulid limestones, which may represent the main Algal 

member of the lyne Formation. However, this has not been 

positively identified. 

Thickness 

in the Bewcastle area, in the central part of the 

Northumberland Trough, the formation is at least 890 m 

thick. However, in Annandale, the Hoddom No. 2 Borehole 

(see above) showed the lyne Formation to be 37.22 m thick. 

in the easton 1 borehole (see above) the easton Anhydrite 

member is more than 1153 m thick (base not seen). 


Northumberland Trough and solway Basin: langholm– 

Bewcastle, and southerness. seismic reflectors suggest that 

the top of the easton Anhydrite member extends at depth 

from west Cumbria eastwards to the flanks of the Bewcastle 

Anticline and beyond (see ward, 1997, fig. 11). 


late Tournaisian to Chadian (waters et al., 2007, p. 18). The 

limestones commonly contain stromatolites and vermetid 

gastropod bioherms and biostromes. in the west quasimarine 

shelly faunas contain abundant brachiopods (including 

Antiquatonia teres). Based on limited palynology, the easton 

Anhydrite member is considered to be early visean in age. 


see also Appendix 1. members of the lyne Formation in 


6.5.1.1 easTon anHyDriTe MeMBer 

Name 

originally named the ‘easton Anhydrite Facies of the 

lower Border Group’ by ward (1997) the unit is here 

formally renamed the easton Anhydrite member. it is 

derived from the easton 1 borehole, which was drilled near 

the hamlet of easton 16 km north of Carlisle, and includes 

the type section. 

Lithology 

Grey or white anhydrite interbedded with limestones, 

shales, siltstones and sandstones. 


The sedimentary rocks are predominantly of shallow water 

origin. They were deposited in a rapidly subsiding basin, 

with restricted marine circulation, in which sedimentation 

and rapid burial is inferred to have kept pace with 

subsidence. most of the anhydrite is likely to have had 

a subaqueous rather than a sabkha origin, the purer and 

thicker beds probably precipitating as gypsum in regionally 

extensive salinas. 

Stratotype 

The partial type section is the easton 1 borehole (BGs 

Registration Number Ny47sw/15) [Ny 44124 71694] 

91 

from 1054 to 2260 m depth (the base of member not being 

proved). An upper unit, 126 m thick, includes successions 

of generally upward-thinning beds of anhydrite, interbedded 

with limestone, some dolostone, sandstone and shale. 

A middle unit, 639 m thick, includes nine large cyclical 

sequences of limestones, shales, sandstones and anhydrite. 

A lower unit, at least 440 m thick, includes composite 

limestone-anhydrite beds, 2.4–6.1 m thick, separated by 

shales or claystones that thicken downwards. sandstones in 

this unit are numerous but thin. 


The base of the member is not seen, but seismic interpretation 

indicates the presence of ‘several thousands of feet’ of 

conformable strata below the succession in some parts of 

the solway Basin (see ward, 1997, p. 283). 

The top of the member is taken where numerous beds 

of anhydrite interbedded with limestones, shales, siltstones 

and sandstones give way to strata with variously algal, 

oolitic, peloidal, shelly, crinoidal and serpulid limestones, 

which may represent the main Algal member of the lyne 

Formation. However, this has not been positively identified. 

Thickness 

more than 1153 m (base not seen). 


solway Basin, proved in the easton 1 borehole (see above). 

The member is not exposed at the surface (breccias present 

suggest it was removed by solution), but seismic reflectors 

suggest that the top of the member extends at depth from 

west Cumbria eastwards to the flanks of the Bewcastle 

Anticline and beyond (see ward, 1997, fig. 11). A total area 

well in excess of 1000 km 2 is inferred. 

Age 

early visean, determined by limited palynology (ward, 

1997). 

6.5.1.2 souTHerness liMesTone MeMBer (solM) 

Name 

previously known as the southerness Beds (Craig, 1956; 

deegan, 1970) and the southerness limestone Formation 

(lintern and Floyd, 2000). The status is changed to that of 

a member. 

Lithology 

interbedded fossiliferous marine limestone, mudstone and 

minor siltstone, with thick beds of bioturbated sandstone 

and prominant algal horizons. see Craig (1956); deegan 

(1970). 

Stratotype 

The partial type section of the southerness limestone 

member occupies a 0.5 km stretch of coast about 400 m west 

of the lighthouse at southerness [NX 968 543 to 973 541]. 

The strata are deformed by a gently north-east plunging 

anticline within the eastern limb of which are exposed some 

135 m of fossiliferous, thin-bedded, calcareous mudstones, 

siltstones and limestones, with four thin beds of calcareous 

sandstone (lintern and Floyd, 2000, p. 78). 


The base is not exposed, but the boundary is probably 

gradational with the thinly interbedded siltstones and 

argillaceous limestones (‘cementstones’) of the Kirkbean 

Cementstone member of the Ballagan Formation (inverclyde 

Group). 



The top of the member has a gradational contact with 

strata of the Gillfoot sandstone member of the Fell 

sandstone Formation (Figure 10, Column 2). 

Thickness 



southerness shore, southerness, Kirkcudbrightshire, southwestern 

scotland (southern uplands). 

Age 

Courceyan to Arundian 

6.5.1.3 lyneBanK MeMBer (lyn) 

Name 

previously known as the lynebank Beds (day, 1970). see 

also leeder (1974). 

Lithology 

Alternations of thin limestones, dolomitic limestones 

(‘cementstones’) and mudstones, with sandstone beds 

towards the top of the sequence. 

Stratotype 

A partial type section including the lower part of the 

lynebank member occurs in the River white lyne between 

ellery sike [Ny 5433 7584] and Nixontown [Ny 5482 

7550]. The upper part of the lynebank member occurs in 

the River Black lyne [Ny 5431 7828 to 5411 7821] southeast 

of Holmehead Farm (day, 1970). 


Base not seen. The upper boundary is conformable at 

the base of the Bogside limestone (BGsl) at the base 

of the Bewcastle member (Figure 11, Column 2) with 

cyclical sequences of sandstone, siltstone, mudstone and 

thin limestones and ‘cementstones’. 

Thickness 

About 430 m at Bewcastle. 


The Northumberland–solway Basin, but described only in 

the Bewcastle region (day, 1970). 

Age 

Chadian 

6.5.1.4 BewCasTle MeMBer (BwCB) 

Name 

previously known as the Bewcastle Beds (day, 1970). 

Lithology 

Cyclical sequences of sandstone, siltstone, mudstone and 

thin limestones, locally dolomitic (‘cementstones’); locally 

thin seatearths, nodular algal limestone and traces of coal 

(see day, 1970; leeder, 1974). 

Stratotype 

A partial type section that includes nearly all of the Bewcastle 

member, from the Bogside limestone to just above a 

probable equivalent of the Junction limestone, is exposed 

in Ashy Cleuch [Ny 5648 7698 to 5808 7665] (day, 1970). 


At Bewcastle, the lower boundary is defined at the base of 

the Bogside limestone (BGsl), and is conformable on the 



92 

alternating thin limestones, ‘cementstones’ and mudstones 

of the lynebank member (Figure 11, Column 2). 

The upper boundary is conformable with the base of the 

lowermost algal bed (m.A.1 of day, 1970) of the rhythmically 

alternating limestone and mudstone with nodular algal 

beds of the main Algal member. 

Thickness 

About 180 m at Bewcastle. 




Age 


6.5.1.5 Main algal MeMBer (Man) 

Name 

previously known as the main Algal limestone Beds (day, 

1970). see also leeder (1974). 

Lithology 

Rhythmic alternations of limestone and mudstone with 14 

well developed nodular algal beds and subsidiary sandstone 

and siltstone. 

Stratotype 

The type section is in Birky Cleuch from [Ny 5885 7540 to 

5932 7538] a tributary of the Kirk Beck at Bewcastle. Here, 

a complete sequence from m.A.1 to m.A.14, about 87 m 

thick is exposed (day, 1970). 


At Bewcastle, the lowermost algal bed (m.A.1 of day, 

1970) of the main Algal member lies conformably on 

the Bewcastle member (Figure 11, Column 2), which 

comprises cyclical sequences of sandstone, siltstone, and 

mudstone, with thin limestones and ‘cementstones’. 

At the top of the main Algal member, the top of the 

uppermost algal bed (m.A.14 of day, 1970) is conformable 

with the overlying lower Antiquatonia Bed (lAQB) of the 

Cambeck member, which comprises rhythmic cycles of 

mainly sandstones, thin limestones and mudstones. 

Thickness 

some 87 m at Bewcastle. 




Age 

Arundian. 

6.5.1.6 CaMBeCK MeMBer (CMBB) 

Name 

previously known as the Cambeck Beds (day, 1970). see 

also leeder (1974). 

Lithology 

Rhythmic cycles of mainly sandstones, thin limestones and 

mudstones (the beds being abundantly shelly), and some algal 

beds and subsidiary siltstone. see day (1970); leeder (1974). 

Stratotype 

partial type sections at Bewcastle include the River white 

lyne [Ny 5116 7300 to 5109 7322] with strata from the

PENNINE COAL 

MEASURES GP 


N 

98001786 

BRAMPTON 

TYNE LIMESTONE FORMATION ALSTON FORMATION STAINMORE FORMATION 


FORMATION 

1 

PENNINE MIDDLE COAL 


M 

PENNINE LOWER 

COAL MEASURES 

FORMATION 

? 

VDMB 

‘Second Grit’ 

‘First Grit’ 

UFTL 

LFTL 

THL 

PHL 

CORL 

BSDL 

OKL 



LTLS 

GL 

FFL 

TYL 

FIVE YARD LIMESTONE 

MEMBER 

SCAR LIMESTONE MEMBER 

CSL 

SPL 

TYNEBOTTOM LIMESTONE 

MEMBER 

JEW LIMESTONE MEMBER 

GGL 

BNKL 

LTL 

DNML 

NL 

NWBB 

LHL 

APL 

MIL 

LANL 

KBL 

LOCALITIES 

1 

Carlisle 

2 

? 

3 

2 

BEWCASTLE AND BRAMPTON 

(NORTH) 


BORDER GROUP 

ALSTON 

FORMATION 



FORMATION 

LYNE FORMATION 

BEWCASTLE 

MEMBER 

93 

GL 

‘Under Limestone’ 

FFL 

EWL 

TMBL 

BRDL 

PNLS 

LTL 

DNML 

NL 

NWBB 

APL 

MIL 

DPL 

LWSL 

CTB 

WBB 

HLAB 

CAMBECK 

MEMBER 

UAQB 

LAQB 

MAIN ALGAL 

MEMBER 

BGSL 

CFL 

LYNEBANK 

MEMBER 

RWNL 

ESL 

? 


3 

BELLINGHAM 

STAINMORE 

FORMATION 

ALSTON FORMATION 


FELL 

SANDSTONE FM 

LYNE FORMATION 

metres 

SCALE 

150 

0 

OKL 

LTLS 

GREAT LIMESTONE 

MEMBER 

FOUR FATHOM 


THREE YARD 


RBUL, RBML, RBLL 

EELWELL 

SWOL LIMESTONE 

UBWL, LBWLMEMBER 

CWELL 

BARL 

OXFORD 

GGL LIMESTONE 

BNKL MEMBER 

LTL 

LOCH 

UDML, LDML 

DNL 

UGFL, LGFLL 

NL/FLL 

NWBB 

RDL 

LCRT 

LHL 

APL 

SHL 

UMIL, LMIL 

KBL 

DSL? 

OKSS? 

‘Algal Limestone’ 

Figure 11 solway Basin. Representative 

sections for Carboniferous strata at Brampton, 

Bewcastle and Brampton (North) and 

Bellingham. Based on Trotter and 

Hollingworth (1932), day (1970), Frost and 

Holliday (1980). The profiled location of the 

numbered sections is given in the inset map. 

see Appendices 1 and 2 for the names of the 

lithostratigraphical units shown by BGs 

lexicon of Named Rock units computer codes. 

Blue colour indicates named limestone beds; 

green colour indicates significant developments 

of named sandstone units. dashed lines 

indicate conjecture. 



lower Antiquatonia Band to the base of the whitberry 

Band, and whitberry Burn [Ny 5220 7404 to 5203 7408] 

with strata from the Barrow’s pike sandstone to the base of 

the whitberry Band (day, 1970). 


At Bewcastle, the base is conformable on the uppermost 

algal bed (m.A.14 of day, 1970) of the main Algal 

member (Figure 11, Column 2), which comprises rhythmic 

alternations of limestone and mudstone with nodular algal 

beds. 

There is a conformable upper boundary with the base 

of the locally developed whitberry Band (wBB) of the 

sandstone-dominated Fell sandstone Formation. 

Thickness 

some 204 m at Bewcastle 




Age 

Arundian to Holkerian. 

6.5.2 Fell Sandstone Formation (FELL) 

Name 

The name is derived from the larriston Fells (peach and 

Horne, 1903). 

Lithology 

The Fell sandstone Formation in the north-east 

Northumberland Trough comprises fine- to medium-grained, 

mica-poor, subarkosic sandstone with sparse interbeds 

of red mudstone (smith, 1967). This passes towards the 

central part of the trough into a continuation of the cyclical 

successions of fine-grained subarkosic sandstone, siltstone, 

mudstone and thin limestone present in the underlying lyne 

Formation, although in the Fell sandstone the sandstones are 

thicker and the limestones thinner (day, 1970). seatearths 

are common in the formation, but only in the upper part. 

Thin olivine basalt lavas occur as the Kershopefoot basalts 

(williamson in stephenson et al., 2003). At southerness, 

members of the formation include the Gillfoot sandstone 

and powillimount sandstone members. in the Colvend 

and Rerrick outliers the formation includes the Rascarrel 

member. 


The sandstone is interpreted as having been deposited 

from both low-gradient meandering rivers and highgradient 

braided perennial rivers, which occupied channel 

belts several kilometres wide along the axial part of 

the Northumberland Trough (Hodgson, 1978). The Fell 

sandstone succession in the central part of the trough 

represents deposition in a mixed fluviodeltaic and shallow 

marine environment. 

Stratotype 

The Fell sandstone Formation reaches its most characteristic 

development in the simonside Hills in the Rothbury area of 

Northumberland (B. young, written communication, 24 

June 2004). Type sections occur at murton High Crags, 

south-west of Berwick-upon-Tweed [NT 9620 4950], on 

the foreshore at Burnmouth [NT 9580 6110], and on the 

River white lyne [Ny 5110 7320]. Further sections occur 

south-west of Berwick-upon-Tweed [NT 9300 4500]. in 



94 

Annandale, the Hoddom No.2 Borehole (BGs Registration 

Number Ny17se/3) [Ny 1641 7285] included the Fell 

sandstone Formation from 41.60 to 102.62 m depth. The 

type section of the Kershopefoot basalts is at Kershopefoot 

Quarry [Ny 5005 8339], but neither the top nor bottom of 

the sequence is seen. 


The base of the Fell sandstone Formation is locally 

unconformable and diachronous on a range of lower 

Carboniferous strata, including the lyne Formation in 

the central parts of the Northumberland Trough (Figure 

8, Column 11). locally, it is defined as the base of 

the whitberry Band (wBB) (Figure 11, Column 2). At 

Brampton, the base of the Fell sandstone Formation 

rests conformably on the Ballagan Formation, inverclyde 

Group (Figure 11, Column 1), but in the north-east part 

of the Northumberland Trough the same boundary is 

unconformable (Figure 8, Column 12). 

The top of the formation is locally unconformable and 

diachronous at the base of the Clattering Band (CTB) of northwest 

Northumberland (Figure 8, Column 11), its correlative 

the Kingsbridge limestone (KBl), or in the langholm area, 

the Glencartholm volcanic Beds (Gv), of the Tyne limestone 

Formation (yoredale Group) (Figure 10, Column 3). 

Thickness 

The formation ranges from 130–300 m thick in the northeast 

of the Northumberland Trough. it is 350–450 m thick 

in the central part of the trough measured between the bases 

of the whitberry and Clattering bands. At Annandale, in 

the Hoddom No. 2 Borehole (see above) the Fell sandstone 

Formation is about 61 m thick. The Kershopefoot basalts 

attain a maximum thickness of about 36.5 m (williamson 

in stephenson et al., 2003). 


Tweed Basin and the northern and central parts of 

the Northumberland Trough–solway Basin, from 

Burnmouth, Berwickshire in the north-east to southerness, 

Kirkcudbrightshire in the south-west. The Kershopefoot 

basalts occur in scattered outcrops south-east of langholm 

between [Ny 40 83 and 50 83]. 

Age 

deposition of the formation occurred earliest in the northeast 

of the Northumberland Trough (Chadian to Holkerian). 

in the central part of the trough, the equivalent strata are of 

Arundian to Holkerian age. 


see also Appendix 1. members of the Fell sandstone 

Formation in ascending stratigraphical order include: 

6.5.2.1 gillFooT sanDsTone MeMBer (gisD) 

Name 

originally named the Gillfoot Beds by Craig (1956), and 

the Gillfoot sandstone Formation by lintern and Floyd 

(2000). 

Lithology 

see Craig (1956); deegan (1970). The member comprises 

interbedded medium- to coarse-grained sandstone and 

subsidiary conglomerate with limestone and siltstone. 

Stratotype 

The type section is Gillfoot Bay, southerness, 

Kirkcudbrightshire [NX 9780 5430 to 9870 5610] where

etween 120 and 150 m of strata, comprised dominantly of 

sandstones and conglomerates with subordinate shales and 

fossiliferous marine beds, are exposed on the shore (Craig, 

1956; lintern and Floyd, 2000). 


The base has a gradational contact with strata of the 

southerness limestone member (Figure 10, Column 2). 

The upper boundary is taken as the top of the uppermost 

conglomerate associated with reddened strata, and is 

gradational with the interbedded mainly sandstone, sandy 

limestone and mudstone of the powillimount sandstone 

member. 

Thickness 



Gillfoot Bay, southerness, Kirkudbrightshire, south-western 

scotland (southern uplands). 


Arundian. Near the top of the member a shelly ‘rib’ yielded a 

fauna (possibly derived) including the coral Siphonodendron 

cf. scoticum and the brachiopod Punctospirifer scabricosta. 

S. scoticum occurs in Arundian to Asbian strata in Britain 

and the faunal evidence suggests that the Gillfoot sandstone 

member is Arundian in age (lintern and Floyd, 2000 and 

references therein). 

6.5.2.2 PowilliMounT sanDsTone MeMBer (PosD) 

Name 

originally named the powillimount Beds and Thirlstane 

sandstone by Craig (1956), and the powillimount sandstone 

Formation by lintern and Floyd (2000). 

Lithology 

see Craig (1956) and deegan (1970). interbedded 

bioturbated sandstone, sandy limestone (with some oncolite 

beds), and sparsely fossiliferous mudstone. There is 

subsidiary siltstone and a trace of coal. 

Stratotype 

The type section is the coast between powillimount Bay 

[NX 9880 5610] and Thirl stane [NX 9925 5690] with 

about 160 m of sandstone, limestone, and mudstone. 

The top 25 m of the member comprise the thick-bedded 

Thirlstane sandstone Beds (lintern and Floyd, 2000). 


The base is gradational and taken where mainly interbedded 

medium- to coarse-grained sandstone and subsidiary 

conglomerate of the Gillfoot sandstone member gives 

way to mainly interbedded bioturbated sandstone, sandy 

limestone and mudstone of the powillimount sandstone 

member (Figure 10, Column 2). 

The top of the member is taken at the top of the Thirlstane 

sandstone, which lies conformably beneath the interbedded 

marine limestone, mudstone and subsidiary siltstone, with 

thick cross-bedded, bioturbated, medium-grained sandstone of 

the Arbigland limestone member, Tyne limestone Formation. 

Thickness 

some 135 m 


powillimount shore, southerness, Kirkcudbrightshire, 

south-western scotland (southern uplands). 

95 

Age 


6.5.2.3 rasCarrel MeMBer (rasC) 

Name 

previously known as the Rascarrel sandstones and 

Conglomerates by Craig and Nairn (1956), and the Rascarrel 

Group by deegan (1973), the status has been changed from a 

formation to a member and the “sandstone” epithet removed. 

Lithology 

Conglomeratic sandstone interbedded with thin beds of 

‘marl’ and siltstone, and subsidiary coal and mudstone. 

Stratotype 

partial type sections include coastal sections between Castle 

muir point [NX 7980 4710] and Rascarrel Burnfoot [NX 

8030 4800] where there are more than 360 m of sandstone, 

‘marl’, and siltstone with thin mudstones and coals; and 

between Castlehill point [NX 8545 5240] and Gutcher’s 

isle [NX 8635 5265] where the sequence includes a basal 

breccia, conglomerate, sandstone and shale, perhaps 21 m 

thick (see Craig and Nairn, 1956; deegan, 1973; lintern 

and Floyd, 2000). 


The base has faulted and unconformable contacts with the 

calcareous greywackes and silty mudstones (hornfelsed 

where they occur within the aureole of the Criffel 

Granodiorite) of the Ross Formation (Hawick Group). 

in the Rerrick outlier the member is faulted against the 

conglomerates, conglomeratic sandstones, sandstones, red 

siltstones, ‘marls’ and pedogenic dolostones (‘cornstones’) 

of the orroland member (Ballagan Formation). 

The top of the member is not seen, and lintern and Floyd 

(2000, p. 86) indicate that no rocks of Namurian or westphalian 

age are present on the Kirkudbright–dalbeatie coast. 

Thickness 



Rascarrel Bay (Rerrick outlier); Castlehill point to Gutcher’s 

isle and portling to portowarren shores (Colvend outlier), 

Kirkcudbrightshire, south-western scotland (southern 

uplands). 

Age 


6.6 GREAT SCAR LIMESTONE GROUP (GSCL) 

The Great scar limestone Group (George et al., 1976; 

see also waters et al., 2007) (Figure 7) of open marine, 

platform and ramp carbonates facies is widespread across 

Northern england. it comprises many formations with 

distinct formation nomenclature for the isolated horst and 

tilt-block highs. 

The Alston Block includes the melmerby scar limestone 

Formation (see dunham, 1990). 

The Stainmore Trough has the Coldbeck limestone, 

scandal Beck limestone, Brownber, Breakyneck scar 

limestone, Ashfell sandstone, Ashfell limestone, potts 

Beck limestone and Knipe scar limestone formations (see 

dunham and wilson, 1985). 



The Askrigg Block includes the Tom Croft limestone, 

Ashfell sandstone, Fawes wood limestone, Garsdale 

limestone and danny Bridge limestone formations (see 


The Askrigg Block–Craven Basin Transition Zone includes 

the Kilnsey, Chapel House limestone, malham and Cracoe 

limestone formations (see Arthurton et al., 1988). 

South Cumbria has the martin limestone, Red Hill 

limestone, dalton, park limestone and urswick limestone 

formations (see Rose and dunham, 1977; Johnson et al., 

2001). 

North and west Cumbria includes the Frizington limestone 

and eskett limestone formations (see Akhurst et al., 1997). 

it therefore includes the lower part of the now obsolete 

Chief limestone Group. 

The south Isle of Man includes the derbyhaven, Knockrushen 

and Balladoole formations (see Chadwick et al., 2001). 

The north Isle of Man includes undifferentiated strata 

assigned to either the Great scar limestone Group or the 

yoredale Group (see Chadwick et al., 2001). 

The succession comprises limestone, typically well washed, 

bioclastic, highly bioturbated with crinoid banks, shelly or 

coral biostromes and algal (Girvanella) bands. The group, 

common to other visean platform areas in the British 

isles, shows a trend from dark grey Arundian to Holkerian 

carbonates to pale grey Asbian to Brigantian limestones 

with eight major palaeokarstic bedding surfaces overlain 

by thin mudstones (waltham, 1971). Apron knoll reefs 

are developed along the southern margin of the Askrigg 

Block. in the stainmore Trough the limestone succession 

locally includes numerous intercalated sandstone 

beds, presumably derived from upstanding areas of lower 

palaeozoic rocks. The lower part of the group, present in 

the stainmore Trough (Coldbeck limestone Formation) 

and south Cumbria (martin limestone Formation), was 

deposited in a carbonate dominated, nearshore to peritidal, 

restricted marine environment with common stromatolites 

and oncolites. younger strata, dominated by thick bioclastic 

limestones, were deposited in an open, shallow marine environment. 

palaeokarst surfaces indicate periodic emergence. 

The alluvial Brownber and fluviodeltaic Ashfell sandstone 

formations represent brief incursions of siliciclastic deposits 

into the stainmore Trough that encroached from the 

north. They may have been a distal extension of the Fell 

sandstone Formation of the Border Group. in the north of 

the isle of man undifferentiated strata assigned to either the 

Great scar limestone Group or the yoredale Group comprise 

massive, stylolitised, fractured and sucrosic dolomite 

(see Chadwick et al. 2001). 

in the stainmore Trough the base of the group is taken 

at the base of the Coldbeck limestone Formation where the 

Algal Nodular Beds of the underlying Ravenstonedale Group 

are conformably overlain by carbonate-dominated strata. 

on the Askrigg Block the base of the group is taken at 

the base of the Tom Croft limestone Formation where a 

nodular dolostone bed with rhizoliths, indicative of emergence 

(Burgess, 1986), is locally developed at the top of 

the underlying penny Farm Gill Formation (Ravenstonedale 

Group). This boundary is disconformable and marks a low 

sea-level stand. 

on the Alston Block the base of the group is taken at 

the base of the melmerby scar limestone Formation where 



96 

the conglomerates of the underlying marsett Formation 

(Ravenstonedale Group) are unconformably overlain by the 

onset of platform carbonate strata. 

in north and west Cumbria the base of the group is taken 

at the base of the Frizington limestone Formation where the 

conglomerates of the marsett Formation (Ravenstonedale 

Group) are disconformably overlain by bioturbated peritidal 

limestones with rhizoliths, lime muds and sandstones. This 

disconformity represents nondeposition during Chadian to 

Arundian times. 

in south Cumbria the base of the group is not exposed, 

but it is taken to be at the base of the martin limestone 

Formation where limestone becomes dominant over shale 

in the conglomeratic marsett Formation (Ravenstonedale 

Group). 

in the south isle of man the base of the group is taken 

at the base of the derbyhaven Formation where the conglomerates 

(some of which are apparently reworked) of 

the langness Conglomerate Formation (Ravenstonedale 

Group) are directly overlain by limestones. 

in most places, the base of the yoredale Group (mixed 

shelf carbonate and deltaic (‘Yoredale’) facies) defines the 

top of the Great scar limestone Group. The exceptions 

include the north isle of man where the millstone Grit 

Group (fluviodeltaic (‘Millstone Grit’) facies) defines the 

top of what may be either the Great scar limestone Group 

or the yoredale Group, and the south isle of man where the 

Craven Group defines the top of the Balladoole Formation. 

The type area of the Great scar limestone Group is the 

Askrigg Block, where it was first formalised as a group by 

George et al. (1976). subsequently the name was expanded 

to unify all equivalent, locally named, thick carbonate 

platform successions of the Tournaisian to early Namurian 

(pendleian) of Northern england (see waters et al., 2007, 

for further details). 

The group is about 107 m thick on the Alston Block 

and Asbian in age. it gains a maximum thickness of about 

800 m in the stainmore Trough where it is Chadian to 

Asbian in age. on the Askrigg Block it is about 400 m thick 

and Arundian to Asbian in age. in Cumbria, up to about 

740 m of Tournaisian to pendleian strata are present, and in 

the south isle of man the group is up to about 157 m thick 

and Arundian to Asbian in age. in the north isle of man 

the approximately 7.3 m of what may be either Great scar 

limestone Group or yoredale Group strata at the base of 

the Ballavaarkish (shellag North) Borehole (see below) are 

possibly early Namurian or visean in age, but diagenesis of 

the sedimentary rocks has completely ruled out obtaining a 

biostratigraphical age (Chadwick et al., 2001). 

ALSTON BLOCK (Figure 9, Column 15): 

6.6.1 Melmerby Scar Limestone Formation (MEL) 

Name 

The name is derived from the melmerby scar on the Alston 

Block. 

Lithology 

see dunham (1990). The formation comprises distinctive 

lower and upper parts. The lower part, the melmerby 

scar limestone, comprises grey, thick bedded limestone 

with generally thin calcareous mudstone partings. These 

apparently pass northward into two or three rhythmic units 

including clastics as well as limestone in the Brampton 

district and Northumberland Trough. The upper part of 

the formation comprises the Robinson limestone, which 

consists of alternations of shale, sandstone and limestone.


marine platform 

Stratotype 

The type area is the pennine escarpment above melmerby. 

Natural sections in the formation occur along the melmerby 

scar escarpment at, for example, longfell, scoredale, 

dufton Fell and Blencarn Beck (see dunham, 1990), and 

also in boreholes as at Roddymoor and emma pit (BGs 

Registration Number NZ13Ne/146) [NZ 1513 3635] and 

Rookhope (BGs Registration Number Ny94sw/1) [Ny 

9375 4278], the depth range in the latter being from about 

344 to 379 m. 


The base of the formation is unconformable on the 

conglomerates of the marsett Formation, Ravenstonedale 

Group (Figure 9, Column 15; Figure 15, Column 1). 

At the top of the formation there is evidence of penecontemporaneous 

erosion and pot-holing at the top of the 

Robinson limestone (RNl). This surface is overlain unconformably 

by siltstone or sandstone of the Tyne limestone 

Formation, yoredale Group. 

Thickness 

The melmerby scar limestone ranges in thickness from 

35–107 m. The Robinson limestone is normally 4–6 m 

thick, but in Augill Beck (approaching the stainmore 

Trough) it is 25 m thick. 


Alston Block. 


Asbian. The equivalent of Garwood’s (1913) ‘Bryozoa 

Band’, encountered in the Garsdale limestone Formation 

of the Askrigg Block, also occurs near the base of the 

melmerby scar limestone Formation (Turner, 1927). The 

late Asbian Cf6 subzone foraminifers Bradyina rotula 

and Endothyranopsis crassa, and alga Ungdarella uralica, 

are examples of those recovered from the melmerby scar 

limestone Formation in the Rookhope Borehole (see 

above) (Cozar and somerville, 2004). 

STAINMORE TROUGH AND RAVENSTONEDALE 

(Figure 9, Column 16): 

6.6.2 Coldbeck Limestone Formation (CLK) 

Name 

The name is derived from Coldbeck, Ravenstonedale, 

westmorland. 

Lithology 

see mitchell (1978); dunham and wilson (1985). The 

formation comprises dark grey, fine-grained, well bedded 

limestones with mudstone partings, and flaggy dolostones 

characterised by an abundance of algal macrostructures 

including stromatolites and oncolites. 


The formation was deposited in a carbonate-dominated, 

nearshore to peritidal, restricted marine environment. 

Stratotype 

The type area is Ravenstonedale (see Taylor et al., 1971; 

mitchell, 1978). 52 m of strata are visible in a continuous 

section in stone Gill [Ny 71 03]. 

97 


The lower boundary is at the base of the ‘spongiostroma 

Band’ of Turner (1950), which overlies the thick-bedded, 

porcellanous limestones and thin-bedded dolostones in 

the upper part of the stone Gill limestone Formation, 

Ravenstonedale Group (Figure 9, Column 16). 

The upper boundary of the Coldbeck limestone 

Formation is at the top of the Algal Nodular Beds. These 

conformably underlie the dark grey limestone of the 

scandal Beck limestone Formation. 

Thickness 

some 52 m of strata are visible in a continuous section 

in stone Gill, Ravenstonedale, but Turner (1950, p. 30) 

estimated that a further 31 m are cut out by faulting. 

The formation is about 50 m thick at Gaisgill, but thins 

westward from here. 


Ravenstonedale, Cumbria and the stainmore Trough. 


early Chadian. There are at least three algal bands within 


6.6.3 Scandal Beck Limestone Formation (SCBL) 

Name 

The name was first proposed by mitchell (1972) and given 

formation status by pattison (1990). 

Lithology 

The scandal Beck limestone Formation largely comprises 

dark grey, fine- to medium-grained, variable but commonly 

quite thin-bedded, packstone. interbeds of sandstone, 

siltstone or mudstone between these fossiliferous limestones 

are common. 


millward et al. (2003) considered the depositional 

environment to be a deep water carbonate ramp. 

Stratotype 

The type area is scandal Beck [Ny 718 040], in the 

Ravenstonedale area. 

Lower and upper and boundaries 

The base of the formation is conformable on the the Algal 

Nodular Beds at the top of Coldbeck limestone Formation, 

the latter comprising well bedded limestones with mudstone 

partings, and flaggy dolostones with algal macrostructures. 

A succession of sandstones, oolitic limestones and layers 

of quartz pebbles, the Brownber Formation (BNBF), conformably 

overlies the scandal Beck limestone Formation 

in Ravenstonedale (Figure 9, Column 16). 

Thickness 

The formation is about 120 m thick at Ravenstonedale, 

thinning to the north-east and south-west. it is about 50 m 

thick in the Appleby district. 


The Ravenstonedale area. 


Chadian to early Arundian? (see mitchell, 1978, fig. 60, 

col. d after Taylor et al., 1971; Ramsbottom in dunham and 

wilson, 1985, p. 28; George et al., 1976, p. 39, fig. 11:4; 



millward et al., 2003, fig. 7). stratigraphically significant 

fossils within the formation include the coral Dorlodotia 

pseudovermiculare. 


see also Appendix 1. members of the scandal Beck 

limestone Formation, in ascending stratigraphical order, 

include: 

6.6.3.1 ParK Hill liMesTone MeMBer (Pal) 

Name 

The name was given by pattison (1990) for the lower part 

of the scandal Beck limestone Formation. 

Lithology 

limestone and dolostone, fine-grained grainstone and 

packstone, dark grey to buff, wavy-bedded, interbedded 

with sandstone, siltstone and mudstone. The limestone 

lacks the common occurrence of corals, typical of the 

overlying Coupland syke limestone member. 

Stratotype 

partial type section is the course of the Rais Beck [Ny 6393 

0681 to 6428 0693], north of Fawcett mill, by the village 

of orton, Cumbria where about 20 m of limestone with thin 

beds of dolostone, sandstone and siltstone near the top of 

the member are patchily exposed (see pattison, 1990). 


in the Ravenstonedale area, the base of the member 

coincides with the top of the Algal Nodular Beds at the top 

of Coldbeck limestone Formation, the latter comprising 

well bedded limestones with mudstone partings, and flaggy 

dolostones with algal macrostructures. 

The top of the member occurs beneath the more regularly 

bedded and fossiliferous packstones with thin mudstone 

and siltstone interbeds of the overlying Coupland syke 

limestone member (Cosl) (Figure 9, Column 16). The 

junction is taken at the top of a 5 m-thick sandstone and 

mudstone unit that forms a topographical depression. 

Thickness 



Ravenstonedale, Cumbria between the m6 road and the 

dent Fault Zone, south of Kirkby stephen. 

Age 

Chadian 

6.6.3.2 CouPlanD syKe liMesTone MeMBer (Cosl) 

Name 

The name was proposed by pattison (1990) for the limestones 

that occur between the park Hill limestone member and the 

Brownber Formation. 

Lithology 

packstone, dark grey, regularly bedded, blocky, partly 

dolomitised and bituminous. Cyclically interbedded with 

thin mudstone and siltstone beds. There are traces of 

chert. The limestone beds are a fairly constant 0.75 m 

thickness. 

Stratotype 

A partial type section is in a stone quarry (working in 

2005) on the B6261 road west of the village of orton, 

Cumbria [Ny 5975 0920]. it occurs as a thick-bedded, 



98 

bituminous limestone (wackestone) (see mcCormac, 2001). 

This differs from similar thick-bedded rocks in disused 

quarries to the west [Ny 5984 0924 and 5924 0968] 

where the blocky limestones are commonly or extensively 

dolomitised (possibly in association with minor faults) and 

geodic (see pattison, 1990; mcCormac, 2001). A reference 

section is stapestones Quarry (disused), Raisbeck, Cumbria 

[Ny 6496 0692] where 11 m of limestone (with some 

dolomitisation) are exposed (see pattison, 1990). 


The base of the member is taken at the top of a 5 m unit 

of interbedded sandstone and mudstone, which forms a 

topographical depression at the top of the underlying park 

Hill limestone member. The junction is nowhere exposed, 

but the interbedded unit was formerly seen in a road 

cutting at [Ny 7248 0448] during the construction of the 

Ravenstonedale By-pass, and the junction was recorded in 

m6 site investigation Boreholes at [Ny 5885 0998]. 

The top of the member is taken at the base of the overlying 

Brownber Formation (Figure 9, Column 16) where there 

is a change from dark grey cyclically bedded limestone to 

pale grey ooidal limestone and calcarenite. 

Thickness 



Ravenstonedale, Cumbria between the m6 road and the 

dent Fault Zone, south of Kirkby stephen. 


Chadian. Colonial corals (notably genus Dorlodotia) are 

common within the member. 

6.6.4 Brownber Formation (BNBF) 

Name 

The name is derived from Brownber, near Newbiggin-onlune, 

westmorland; see Tiddeman (in Aveline and Hughes, 

1888); mitchell (1978); pattison (1990); millward et al. 

(2003). 

Lithology 

The sedimentary rocks of the Brownber Formation comprise 

interbedded sandstone (fine-grained, pale brown, laminated 

in part), limestone (calcarenites, grainstones, oolitic in part) 

and dolostone (yellow and flaggy) containing abundant 

quartz pebbles in distinctive and laterally discontinuous 

beds near the top. 


interpretations include a shoreline (beach) deposit 

(Barraclough, 1983; leeder, 1988) and deposition in a tidal, 

high and low energy environment (millward et al., 2003). 

Stratotype 

Reference sections occur in old quarries north of Bousfield, 

park and dawns [Ny 6102 0922 to 6107 0924] including 

beds of limestone and sandstone (with gaps), at or near the 

top of the formation, 4.8 m thick; and in a stream section 

north of orton village Green from [Ny 6241 0844 to 6243 

0851] which includes sandstone and limestone (with gaps) 

6.7 m thick (see pattison, 1990). 


The sandstones of the Brownber Formation overlie limestones 

of the Coupland sike limestone member (scandal Beck

limestone Formation) (Figure 9, Column 16), but the 

boundary is poorly known in the Ravenstonedale area (see 

pattison, 1990; mcCormac, 2001). 

within the stainmore Trough, an unconformity is present 

at the base of the overlying dark grey limestone of the 

Breakyneck scar limestone Formation which comprises 

packstone or grainstone with mudstone/siltstone interbeds. 

Thickness 

About 15–80 m thickness is recorded in the orton area with 

10–40 m in the Appleby district. 


The Ravenstonedale, shap and Appleby area. 

Age 

Chadian (millward et al., 2003) or Arundian (George et al., 

1976, pp. 38–39, fig. 11, col. d; mitchell, 1978, pp. 172– 

173, fig. 60, col. d after Taylor et al., 1971). 

6.6.5 Breakyneck Scar Limestone Formation (BRE) 

Name 

The name is derived from Breakyneck scar, scandal Beck, 

Ravenstonedale and was proposed by pattison (1990). 

it replaces such terms as the Blea Tarn and Tarn sike 

limestones of Garwood (1913), and the ‘Michelinia grandis 

Beds’ of George et al. (1976). similar in lithology and 

identical in age range to the Tom Croft limestone Formation 

of the Askrigg Block (see below), it may be argued that 

either one or the other of these formation names be deemed 

redundant. However, whilst BGs is not actively working on 

these successions rationalisation must be deferred. 

Lithology 

The Breakyneck scar limestone Formation comprises dark 

grey, unevenly (commonly rubbly) bedded, fine- to coarsegrained 

fossiliferous packstone or grainstone with dark grey 

mudstone/siltstone interbeds. 


shallow marine–transgressive carbonates. 

Stratotype 

The type section is exposed in the valley of scandal Beck, 

Ravenstonedale, Cumbria, where there is an estimated 

150 m thickness of mainly limestones with interbedded 

mudstones (see pattison, 1990). The contact with the 

underlying Brownber Formation is exposed near orton [Ny 

6103 0923 to 6125 0925]. A locality in the Appleby district 

is Ravensworth Fell [Ny 597 098] where calcarenites of 

the Brownber Formation are overlain by coarse-grained 

fossiliferous limestone (see mcCormac, 2001). 


The formation unconformably overlies the interbedded 

sandstone, limestone and dolostone of the Brownber 

Formation within the stainmore Trough. 

The top of the formation, beneath the overlying Ashfell 

sandstone Formation cannot be described precisely due to 

poor exposure (see pattison, 1990). 

Thickness 

up to 150 m thick in the east of Ravenstonedale the 

formation thins westwards, pinching out along the line of 

the Anne’s well Fault at [Ny 584 115] (mcCormac, 2001). 

it is about 75 m thick north of Newbiggin-on-lune, and 

about 25 m thick near Howe Nook, orton. 

99 


Ravenstonedale, stainmore Trough. 


early Arundian (George et al., 1976; mitchell, 1978; 

millward et al., 2003). The limestones contain a rich fauna 

including the corals Siphonodendron martini, Palaeosmilia 

murchisoni and Syringopora sp., the productoid Linoprotonia 

sp. and costate spiriferoids. 

6.6.6 Ashfell Sandstone Formation (AFS) 

Name 

The name is derived from Ashfell in Ravenstonedale; 

see Garwood (1913); Turner (1950; 1959); Ramsbottom 

(1973); mitchell (1978); dunham and wilson (1985); 

millward et al. (2003). 

Lithology 

The Ashfell sandstone Formation comprises thick-bedded, 

fine-grained sandstone with current ripple laminations, rare 

cross-bedding, and convolute bedding. interdigitating are 

beds of marine mudstone and thin limestone with shelly 

faunas. 


The fluviodeltaic, marine-regressive, Ashfell sandstone 

Formation represents an incursion of siliciclastic deposits 

into the stainmore Trough encroaching from the north-east. 

it may be a southern and western, distal extension of the 

Fell sandstone Formation, Border Group. 

Stratotype 

The longest and most complete section through the 

formation is along the scandal Beck in the Ravenstonedale 

area, where up to 160 m of sandstone with four limestone 

interbeds occurs (see pattison, 1990; dunham and wilson, 

1985). 


The base of the formation overlying the Breakyneck scar 

limestone Formation cannot be defined precisely due to 

poor exposure. 

The top of the formation conformably underlies the 

mainly packstone, shelly grainstone or lime mudstone 

of the Ashfell limestone Formation in the stainmore 

Trough (Figure 9, Column 16) and shap, east Cumbria 

(Figure 14, Column 3), and the mainly biomicrosparites 

and biomicrites of the Fawes wood limestone Formation 

on the Askrigg Block (Figure 9, Column 17; Figure 15, 

Column 3). 

Thickness 

The formation is 152 m thick in the Ravenstonedale 

area, thinning northwards. in the Raydale Borehole 

(BGs Registration Number sd98sw/1) [sd 9026 8474] 

it is 38.40 m thick. in the Appleby district it is 20–40 

m thick. 


The formation extends from the edge of the lake district to 

the Alston Block, including the eden valley and northern 

margin of the stainmore Trough. 


late Arundian. Fossils of the thin limestone beds include 

the corals Diphyphyllum smithi and Siphonodendron 

martini. 



6.6.7 Ashfell Limestone Formation (AFL) 

Name 

The name is derived from Ashfell in Ravenstonedale, 

Cumbria; see Ramsbottom (1973); George et al. (1976); 

mitchell (1978); dunham and wilson (1985); pattison (1990). 

Lithology 

The distinctive Ashfell limestone Formation is 

characteristically dark grey to dark blue-grey and mainly 

a packstone, shelly grainstone or lime mudstone. strongly 

cross-bedded units, with thin interlaminae of siltstone and 

fine-grained sandstone occur at the base of the formation. 

Convolute beds and nodules of dark grey chert occur 

locally, and partial dolomitisation is common. The top 

of the formation is marked by the presence of dark grey, 

cross-bedded, coarse-grained crinoidal grainstone, grey 

mudstone with bivalves, and vuggy porcellanous limestone 

(the ‘Bryozoa Band’ of Garwood, 1913). 


shallow marine, perhaps slightly restricted carbonate 

environment. 

Stratotype 

partial type sections occur in potts valley [Ny 6988 0827], 

[Ny 6981 0820] and [Ny 6972 0805 to 6969 0813] where 

more than 48 m of limestones in the upper and middle parts 

of the formation are exposed, and at ewe Fell [Ny 6971 

0702 to 6999 0711] where 60 m of the lowest part of the 

formation, comprising limestone and 7 m of sandstone, are 

exposed (see pattison, 1990). 


The mainly packstone, shelly grainstone or lime mudstone 

of the Ashfell limestone Formation conformably overlies 

the sandstones, mudstones and thin limestones of the 

Ashfell sandstone Formation. 

on the northern margin of the stainmore Trough, the 

‘Bryozoa Band’ (BZB) at the top of the Ashfell limestone 

Formation is overlain either conformably by the mainly sparry 

packstone of the potts Beck limestone Formation (Figure 

9, Column 16), or disconformably by the rhythmically bedded 

limestone (mainly wackestone and packstone) of the 

Knipe scar limestone Formation (Figure 14, Column 3). 

Thickness 

The formation is 40–50 m thick at penrith and Brough, but 

thickens to 100 m in the stainmore Trough. 


penrith, Brough and the stainmore Trough. 


Holkerian. shelly beds contain stromatolite colonies, 

coral fragments (including Lithostrotion minus), bryozoa, 

brachiopods (including rhynchonellids, spiriferoids and 

Davidsonina carbonaria), gastropods, crinoid ossicles, 

fish scales and burrows. The characteristic Holkerian 

brachiopod Davidsonina carbonaria is found in the orton 

and Ravenstonedale area (pattison, 1990). The ‘Bryozoa 

Band’ of Garwood (1913) occurs at the top of the formation. 

6.6.8 Potts Beck Limestone Formation (PBK) 

Name 

The name is derived from potts Beck near Ravenstonedale, 

Cumbria (see George et al., 1976). 



100 

Lithology 

see mitchell (1978); dunham and wilson (1985); millward 

et al., (2003). The potts Beck limestone Formation is 

composed largely of pale grey, thick-bedded, strongly jointed, 

sparry packstone. Rubbly weathered calcrete horizons are 

present, as are subordinate sandstones and mudstones. 


marine. 

Stratotype 

The type section is at Great Kinmond [Ny 6728 0892 

to 6728 0927] where some 39 m of mostly fossiliferous 

limestone is exposed. The type area is at little Asby 

scar [Ny 6988 0827] on the north side of potts valley, 

near Newbiggin-on-lune, Cumbria where the base of the 

formation is exposed. 


The base of the formation is conformable, and taken at 

the change from dark grey, cross-bedded, coarse-grained, 

crinoidal grainstone with mudstone interbeds (the ‘Bryozoa 

Band’ of Garwood, 1913) at the top of the underlying 

Ashfell limestone Formation (Figure 9, Column 16), to 

grey, coralline packstone. 

The upper boundary of the formation is overlain by the 

grey, scar-forming, rhythmically bedded, limestone (mainly 

wackestone and packstone) of the Knipe scar limestone 

Formation. 

Thickness 

The formation is up to 45 m thick in the stainmore Trough, 

but thins rapidly towards the surrounding block areas. it is, 

for example, absent north of shap village. 




latest Holkerian to early Asbian. Fossils, which can be 

abundant, include the corals Axophyllum sp., Dibunophyllum 

bourtonense, Palaeosmilia murchisoni, Siphonodendron 

junceum and S. martini, and the brachiopods Daviesiella 

llangollensis and Gigantoproductus sp. The stainmore 

Trough includes the basal Asbian stratotype at little Asby 

scar [Ny 6988 0827] (George et al., 1976). Faunal analysis 

of this section places the Holkerian/Asbian boundary above 

the base of the formation (Ramsbottom, 1981). 

6.6.9 Knipe Scar Limestone Formation (KNL) 

Name 

The name is derived from Knipe scar, Bampton, Cumbria. 

see mitchell (1978). 

Lithology 

The Knipe scar limestone Formation is wholly dominated 

by rhythmically bedded limestone, comprising mostly thickbedded, 

pale to mid grey, wackestone and packstone, with 

some grainstone. palaeokarst horizons and conspicuous 

stratiform mottled calcrete textures in beds up to 1 m thick 

are present. significant beds of fine-grained sandstone, 

siltstone and mudstone punctuate the upper part of the 

succession, but are rarely seen at outcrop. The formation is 

the equivalent of the melmerby scar limestone Formation 

of the Alston Block and the danny Bridge limestone 

Formation of the Askrigg Block and forms spectacular 

scenery of terraced topography and limestone pavements.


shallow marine. The palaeokarst horizons and stratiform 

mottled calcrete textures indicate emergence of the 

unconsolidated carbonate substrate. 

Stratotype 

The formation is exposed in its entirety on the pavements 

of Great Asby scar [Ny 650 100] and Knipe scar [Ny 528 

193]. The type area is Great Asby scar [Ny 6592 0917 

to 6630 0969] where some 50 m of largely thick-bedded 

and mostly bioclastic limestone is exposed. major new 

exposures are available in quarries at Hardendale [Ny 

587 138] and shap Beck [Ny 550 183], where continuous 

sections show thin sandstone and mudstone interbeds in the 

limestone sequence (see pattison, 1990). 


in Ravenstonedale and the stainmore Trough the 

formation conformably overlies the packstones of the 

potts Beck limestone Formation (Figure 9, Column 16). it 

disconformably overlies the ‘Bryozoa Band’ at the top of 

the Ashfell limestone Formation on the northern stainmore 

Trough margin. 

The top of the formation is disconformably overlain by 

a variable sandstone and mudstone unit known locally as 

the wintertarn sandstone member (wTRs) at the base of 

the Tyne limestone Formation, yoredale Group (Figure 9, 

Column 16; Figure 14, Column 3). 

Thickness 

The formation is up to 50 m thick at Knipe scar, but 

thickens to 100 m at Ravenstonedale. 


Ravenstonedale and the stainmore Trough. 


late Asbian. The formation is not abundantly fossiliferous 

in the stainmore Trough, but includes Siphonodendron 

pauciradiale, Davidsonina septosa and Delepinea sp. in 

the eamont valley [Ny 490 260] it is conspicuously 

fossiliferous containing large broken stromatolite colonies, 

Hexaphyllia sp., Lithostrotion sp. and Siphonodendron sp. 

and Gigantoproductus sp. 

ASKRIGG BLOCK (Figure 9, Column 17; Figure 15, 

Column 3): 

6.6.10 Tom Croft Limestone Formation (TCL) 

Name 

The formation was first proposed by Burgess (1986). The 

name is derived from Tom Croft wheel [sd 6948 9147], 

Garsdale, yorkshire. similar in lithology and identical in 

age range to the Breakyneck scar limestone Formation (see 

above) of the Ravenstonedale area, it may be argued that 

either one or the other of these formation names be deemed 

redundant. However, whilst BGs is not actively working on 

these successions rationalisation must be deferred. 

Lithology 

The Tom Croft limestone Formation comprises mid to 

dark grey, poorly bedded biosparites (grainstone containing 

peloids, shelly debris, crinoid fragments and variable quantities 

of dolomite grains). The formation includes a macrofauna 

comparable with that of the ‘dalton Beds’ of south Cumbria 

(see Rose and dunham 1977) and may include a thin basal unit 

of limestone breccia with siltstone and quartz pebbles. 

101 


shallow marine carbonate. 

Stratotype 

Reference sections in the formation include: the River 

Clough [sd 6954 9143 to 6947 9147], Garsdale, where 

the lowest beds are cut out by faults (Burgess, 1986, p. 7) 

but there is an 80 m-thick run (possibly including some 

repetition) of dominantly dark grey limestone virtually free 

of mudstone partings (Burgess, 1986, p. 8; see dunham 

and wilson, 1985, p. 28); the Beckermonds scar Borehole 

(BGs Registration Number sd88se/1) [sd 8636 8016] 

from 209.15 to 267.88 m depth including dominantly dark 

grey limestone with some mid grey runs (see wilson and 

Cornwell, 1982); and the BGs Raydale Borehole (BGs 

Registration Number sd98sw/1) [sd 9626 8474] from 

about 273 to 350 m depth (see dunham and wilson, 1985, 

fig. 5, cols. 5 and 7). 


The base of the formation is disconformable on the 

limestone, dolostone, sandstone and siltstone of the penny 

Farm Gill Formation, Ravenstonedale Group (Figure 9, 

Column 17). 

The top of the formation underlies the diachronous 

Ashfell sandstone Formation in the stainmore Trough 

and the same formation and the Fawes wood limestone 

Formation on the Askrigg Block (Figure 15, Column 3). 

Thickness 

The formation is 60–80 m thick. 




Arundian. The macrofauna includes the corals 

Koninckophyllum sp. and Michelinia megastoma, and the 

brachiopod Delepinea carinata. 

6.6.11 Ashfell Sandstone Formation (AFS) 


6.6.12 Fawes Wood Limestone Formation (FWL) 

Name 

The name is derived from Fawes wood [sd 6955 9145], 

on the River Clough, Garsdale, yorkshire (see dunham and 

wilson, 1985 and references therein). The formation was 

first proposed by Burgess (1986). 

Lithology 

The Fawes wood limestone Formation comprises mid to 

dark grey biomicrosparites and biomicrites (calcarenite, 

mainly grainstone and packstone) with silty or stylolitic 

partings and some porcellaneous micrites. 


shallow marine carbonate 

Stratotype 

Reference sections in the formation include: the River 

Clough, Garsdale [sd 6967 9129 to 6961 9134] where 

the formation comprises biomicrites and medium-grained 

limestones 80.77 m thick (Burgess, 1986, p. 11; dunham 

and wilson, 1985, p. 28); part of the Beckermonds scar 

Borehole (BGs Registration Number sd88se/1) [sd 8636 



8016] from about 143 to 200 m depth, where it comprises 

mid–dark grey limestone, chiefly medium-grain calcarenite 

(wilson and Cornwell, 1982, p. 64); and the BGs Raydale 

Borehole (BGs Registration Number sd98sw/1) [sd 9626 

8474] from about 158 to 235 m depth. dunham and wilson 

(1985, p. 28, see also fig. 5, cols. 5 and 7) summarised the 

formation as comprising about 56–81 m of dominantly dark 

grey and grey fine-grained grainstones and packstones with 

a few mudstone and siltstone beds. 


The formation conformably overlies the sandstones of 

the Ashfell sandstone and biosparites of the Tom Croft 

limestone formations (Figure 9, Column 17; Figure 15, 

Column 3). 

The formation is conformably overlain by the limestones 

with interbedded sandstones, siltstones and numerous thin 

beds of mudstone of the Garsdale limestone Formation. 

Thickness 

The formation ranges in thickness from 80.77 m in the 

River Clough to 55.80 m in the Beckermonds scar Borehole 

(dunham and wilson, 1985). 




Holkerian. Fossils include Siphonodendron martini, 

Linoprotonia sp., and ?Macrochilina sp. The lower part of 

the formation contains distinctive Holkerian assemblages 

with Lithostrotion minus, Siphonodendron sociale and 

Davidsonina carbonaria. Although it is lithologically 

similar to the Ashfell limestone Formation, the upper limit 

of the Fawes wood limestone Formation is taken at a lower 

stratigraphical level. 

6.6.13 Garsdale Limestone Formation (GAL) 

Name 

The name is derived from Garsdale [sd 73 90], yorkshire 

(see dunham and wilson, 1985 and references therein). 

Lithology 

The Garsdale limestone Formation comprises dark grey 

biomicrosparites to porcellanous micrites (wackestone 

with bands of porcellaneous calcilutite) with interbedded 

sandstone and siltstone, numerous thin mudstone beds and 

rare thin coals. Three coal seams, up to 0.07 m thick, occur 

in the Beckermonds scar Borehole (see below). minor 

fenestral and palaeokarst surfaces occur. The formation 

contains the equivalent of Garwood’s (1913) ‘Bryozoa 

Band’. 


shallow marine carbonates (with some intertidal deposits). 

Stratotype 

The type section is the River Clough [sd 6977 9128 to 6967 

9129] in Garsdale, comprising a variety of limestones with 

interbedded sandstones and siltstones, and a thin coal (see 

Burgess, 1986, pp. 11–12). Reference sections include the 

Beckermonds scar Borehole (BGs Registration Number 

sd88se/1) [sd 8636 8016] from about 101 to 143 m depth, 

including dark grey wackestones with beds of calcilutite, 

three thin coal seams, and beds of mudstone concentrated 

near the top of the unit (see wilson and Cornwell, 1982), 

and the BGs Raydale Borehole (BGs Registration Number 



102 

sd98sw/1) [sd 9626 8474] from about 103 to 158 m 

depth. dunham and wilson (1985, p. 28, see also fig. 5 cols. 

5 and 7) described the formation as comprising dominantly 

dark grey, fine-grained wackestone with many interbeds of 

siltstone and mudstone, and one to four thin coal seams and 

seven to ten beds of calcilutite up to 1.22 m thick. 


The conformable base of the formation overlies the mid 

to dark grey limestones of the Fawes wood limestone 

Formation (Figure 9, Column 17; Figure 15, Column 3). 

The top of the formation is conformable beneath the 

pale to mid grey limestone of the danny Bridge limestone 

Formation. 

Thickness 

The formation is 41–58 m thick (dunham and wilson, 

1985). 


Askrigg Block and wharfedale. 


late Holkerian to early Asbian. The equivalent of Garwood’s 

(1913) ‘Bryozoa Band’ includes Pleuropugnoides 

pleurodon, Productus garwoodi, Punctospirifer scabricosta, 

Leiopteria lunulata and ostracods. dunham and wilson 

(1985) considered that the Holkerian–Asbian boundary 

should occur within the Garsdale limestone Formation 

as defined at little Asby scar (see George et al., 1976). 

As such it has no direct lithological, or time equivalent, 

correlative within the nearby Holkerian/Asbian succession 

of Ravenstonedale. 

6.6.14 Danny Bridge Limestone Formation (DBL) 

Name 

The name is derived from danny Bridge [sd 6982 9128], 

Garsdale, yorkshire (see dunham and wilson, 1985, 

and references therein). The formation was proposed by 

Burgess (1986). 

Lithology 

The danny Bridge limestone Formation consists of pale to 

mid grey biosparites and biopelsparites (mainly wackestone, 

with packstone and minor grainstone), and subordinate 

mudstone in 10 regularly spaced interbeds. palaeokarst 

surfaces overlain by bentonitic clays, palaeosols and 

calcareous laminated crusts are common and the formation 

displays a characteristically stepped landscape. 


shallow marine carbonates (emergent at times). 

Stratotype 

The type section of the formation is the River Clough at 

Garsdale [sd 7000 9118 to 6977 9128], which consists 

mainly of marine limestone (biomicrite, biomicrosparite, 

biosparite) and mudstone (see Burgess, 1986, pp. 13–14). 

Reference sections include the Beckermonds scar Borehole 

(BGs Registration Number sd88se/1) [sd 8636 8016] 

from about 8.0 to 101 m depth with mainly pale grey (and 

subordinate mid grey) limestone, thin mudstone or siltstone 

beds, and a section of mineralised flats (see wilson and 

Cornwell, 1982, pp. 61–63; dunham and wilson, 1985, 

fig. 5, col. 5), and the BGs Raydale Borehole (BGs 

Registration Number sd98sw/1) [sd 9626 8474] from 

about 5 to 103 m depth. dunham and wilson (1985, fig. 5,

col. 7) summarised the Raydale Borehole and surface 

exposures as a largely complete sequence about 127 m 

thick with mainly pale grey limestone and thin mudstone 

or siltstone beds. 


The base of the formation is conformable on the dark grey 

limestone of the Garsdale limestone Formation (Figure 9, 

Column 17). 

The cross-bedded, regressive sandstones of the wintertarn 

sandstone member (wTRs), marking the base of the Tyne 

limestone Formation, yoredale Group, overlie the top 

of the danny Bridge limestone Formation (Figure 15, 

Column 3). 

Thickness 

The formation is 102–168 m thick, the greatest thickness 

being on the southern margin of the Askrigg Block (see 



Askrigg Block, wensleydale and wharfedale. The formation 

is the direct equivalent of the Knipe scar and urswick 

limestone formations of the stainmore Trough and south 

Cumbria respectively. 


late Asbian. Amongst the general shelly debris, fossils 

include Davidsonina septosa and typically, Siphonodendron 

martini. The formation also yields a diagnostic late Asbian 

assemblage of foraminifers (see dunham and wilson, 1985, 

p. 22). 

ASKRIGG BLOCK–CRAVEN BASIN TRANSITION 

ZONE (Figure 15, Column 6) 

6.6.15 Chapel House Limestone Formation (CHPL) 

Name 

see Arthurton et al. (1988); murray (1983). 

Lithology 

The lower part of the succession is dominated by mid to 

mid–pale grey, medium- and coarse-grained calcarenite, 

oolitic grainstones interbedded with conglomerates, ‘mixed 

laminites’ (interbedded siltstone with sandstone and 

mudstone laminae), dolomicrites and fenestral or algal 

lime-mudstones. Argillaceous wackestones occur locally in 

the upper part of the formation. 


shallow marine (see murray, 1983). 

Stratotype 

The type section is the Chapel House Borehole (BGs 

Registration Number sd96Ne/1) [sd 9726 6647], near 

Kilnsey, yorkshire, which records the entire thickness of 

the formation (33.8 m) from 56.3 to 90.1 m depth (see 

Arthurton et al., 1988). 


The base is drawn at the base of the conglomerate of the 

Chapel House limestone Formation where it rests with 

significant non-sequence on the deeply fissured limestone 

top surface of the stockdale Farm Formation (Figure 15, 

Column 6), which comprises limestone, siltstone and 

mudstone. it lies directly on lower palaeozoic rocks 

elsewhere. 

103 

The top of the formation is drawn at the sharp conformable 

upward passage from grainstone of the Chapel House 

limestone Formation to darker limestones of the scaleber 

Force limestone member (Kilnsey Formation). 

Thickness 

maximum of about 56 m adjacent to the middle Craven 

Fault, and 33.8 m thick in the type section (see above). 


A series of inliers in the southern part of the Askrigg 

Block, North yorkshire, including Gordale Beck [sd 91 

65], stainforth Force, River Ribble [sd 82 67], and Barrel 

sykes, north of settle [sd 82 64]. The formation is proved 

elsewhere in the subsurface of the settle area in boreholes. 


Arundian. Arthurton et al. (1988) record the presence of the 

corals Michelinea megastoma and Palaeosmilia murchisoni 

from the top and base of the formation respectively, and the 

foraminifers Ammarchaediscus bucullentus, Eoparastaffella 

simplex, Glomodiscus miloni, Latiendothyranopsis menneri 

solida and Rectodiscus sp., which confirm its Arundian age. 

6.6.16 Kilnsey Limestone Formation (KLSL) 

Name 

see mundy and Arthurton (1980) and Arthurton et al. 

(1988). Kilnsey Crag occurs in north yorkshire near the 

Hamlet of Kilnsey, north of skipton. 

Lithology 

The formation comprises dark to mid–pale grey, thick to 

thin-bedded, bioclastic limestone with mudstone beds and 

partings. 


marine. 

Stratotype 

see Arthurton et al. (1988). The partial type section is 

at Kilnsey Crag [sd 9735 6846] near malham, North 

yorkshire, with 8 m of the upper part of the scaleber Force 

limestone member and 29 m of the overlying scaleber 

Quarry limestone member. A reference section is in the 

stockdale Farm (Cominco s7) Borehole (BGs Registration 

Number sd86se/6) [sd 8541 6378] near settle, North 

yorkshire with the formation present from 15.2 to 120.1 m 

depth, which includes 61.6 m thickness of the scaleber 

Force limestone member and 43.2 m in the scaleber 

Quarry limestone member. 


The lower boundary of the formation is drawn at the base 

of the dark grey limestones with mudstone partings of the 

scaleber Force limestone member where it rests sharply 

and conformably on paler grainstone of the Chapel House 

limestone Formation (Figure 15, Column 6). 

The upper boundary of the formation is drawn at the 

conformable upward passage from mid–dark grey limestone 

of the scaleber Quarry limestone member to pale 

grey limestone of the Cove limestone member, malham 

Formation. 

Thickness 

The maximum thickness is about 224 m in boreholes south 

of the middle Craven Fault. The formation thins rapidly 

northwards to 53 m in the Kilnsey area. 




limited to a series of inliers in the southern part of the 

Askrigg Block, North yorkshire including Kilnsey [sd 97 

68], langcliffe [sd 82 65], and Austwick [sd 77 68]. 


Arundian to Holkerian. Biostratigraphically important 

fossils recorded within the formation include foraminifers 

(diagnostic of both stages), Delepinea carinata (which is 

characteristic of the Arundian), and Lithostrotion sensu 

stricto (cerioid), which is not recorded below the base of the 

Holkerian (mitchell, 1989). 


see also Appendix 1. members of the Kilnsey Formation in 


6.6.16.1 sCaleBer ForCe liMesTone MeMBer (sFlM) 

Name 

The name is derived from scaleber Force [sd 8407 6256]. 

it was previously known as the Kilnsey limestone-withmudstone 

member and originally defined by Hudson 

(1930). Arthurton et al. (1988) is the principal reference. 

Lithology 

Bioturbated, well-bedded, fine- to coarse-grained dark 

limestones (packstones and subordinate wackestones), 

generally argillaceous with common detrital quartz, and 

with common mudstone partings and interbeds up to 1.8 m 

thick. 

Stratotype 

The type locality is scaleber Force [sd 8407 6256] 

where a 22 m section is exposed. A reference section is 

the Cominco s7 Borehole (BGs Registration Number 

sd86se/6) [sd 8541 6378] near settle, North yorkshire, 

which includes the full thickness of the member from 58.5 

to 120.1 m depth. 


The base of the scaleber Force limestone member is drawn 

where the dark limestones rest sharply and conformably on 

paler grainstone of the Chapel House limestone Formation 


The top of the member is taken where the dark grey 

limestones of the scaleber Force limestone member are 

overlain by mid–dark grey limestone of the scaleber Quarry 

limestone member. 

Thickness 

North of the middle Craven Fault the member is 22–58 m 

thick. south of the fault it is 61.6 m thick at the type locality 

(see Stratotype above). 


The member occurs in a series of inliers in the southern part 

of the Askrigg Block, North yorkshire, including Kilnsey 

[sd 97 68], langcliffe [sd 82 65], and Austwick [sd 77 68]. 

Age 

Arundian. 

6.6.16.2 sCaleBer Quarry liMesTone MeMBer (sQlM)) 

Name 

The name is derived from scaleber Quarry [sd 9225 5328]. 

it was previously known as the Kilnsey limestone and originally 

defined by Hudson (1930). Arthurton et al. (1988) is 

the principal reference. 



104 

Lithology 

well-bedded, thin and thick beds of mid and mid–dark grey, 

fine- to coarse-grained limestone, with minor mudstone 

beds. Bioclastic packstones characterise the lower part of 

the member, passing up to packstones and grainstones. 

Bands and nodules of black chert occur locally in the lower 

part of the member. 

Stratotype 

The type locality is scaleber Quarry [sd 8407 6263] where 

a 12 m section 18 m above the base of the member is 

exposed. Reference sections are provided by the Cominco 

s2 Borehole (BGs Registration Number sd86sw/6) [sd 

8491 6345] at low Barn, stockdale Beck, from 224.2? 

to 363.9? m depth, and Kilnsey Crag [sd 9735 6846] 

where 29 m are exposed at outcrop in a cliff section. 

Both reference sections include the top and base, and full 

thickness, of the member. 


The base is taken where the mid grey limestone of the 

scaleber Quarry limestone member overlies the dark grey 

limestone and mudstones of the scaleber Force limestone 

member (Figure 15, Column 6). This boundary is typically 

gradational and for convenience the base is taken at the top 

of the highest prominent mudstone. 

The top of the member is drawn at the conformable, 

gradational and slightly diachronous upward passage from 

mid–dark grey limestone of the scaleber Quarry limestone 

member to the pale grey limestone of the Cove limestone 

member (malham Formation). 

Thickness 

up to 134 m thick in the Cominco Borehole s2, decreasing 

to 29 m at Kilnsey Crag (see above). 


The member occurs in a series of inliers in the southern part 

of the Askrigg Block, North yorkshire, including Kilnsey 

[sd 97 68], langcliffe [sd 82 65] and Austwick [sd 77 

68]. 


Holkerian. The member contains an abundant macrofauna 

characterised by cerioid and fasciculate lithostrotionid 

corals. 

6.6.17 Malham Formation (MALM) 

Name 

see Arthurton et al. (1988) and mundy and Arthurton 

(1980). malham Cove [sd 8975 6411] occurs in yorkshire 

near the village of malham, east of settle. 

Lithology 

The formation includes massive- to weakly bedded, 

pale grey to very pale grey, medium- to coarse-grained 

calcarenite packstones and grainstones, and well bedded, 

thick- to very thick-bedded, mid–pale to very pale grey, 

calcarenite packstones, wackestones and subordinate 

grainstones. 


limestone deposition on a rimmed marine shelf. The Cove 

limestone member in shallow water well within fairweather 

wave-base, and the Goredale limestone member in 

cyclical shallow water with emergent episodes (see Cossey 

and Adams, fig. 5.21 in Cossey et al., 2004).

Stratotype 

partial type sections occur at malham Cove [sd 8975 

6411], North yorkshire, where 72 m of the upper part of the 

Cove limestone member, including the top, is present, and 

at Gordale scar [sd 913 640] where the complete thickness 

(94 m) of the Gordale limestone member, including its top 

and base, is seen. see Arthurton et al. (1988). 


The lower boundary of the formation is drawn at the base 

of the pale grey limestone of the Cove limestone member 

where it rests conformably (but gradationally and slightly 

diachronously) on the mid–dark grey limestone of the 

scaleber Quarry limestone member, Kilnsey Formation 

(Figure 15, Column 6), or locally, unconformably on lower 

palaeozoic strata. 

The conformable upper boundary of the formation is 

drawn at the upward passage from pale grey limestone of 

the Gordale limestone member to darker grey limestone 

of the lower Hawes limestone at the base of the Alston 

Formation, yoredale Group. However, in the Cominco s11 

Borehole (BGs Registration Number sd86se/5) [sd 8590 

6340] the upper boundary of what is probably the malham 

Formation is unconformable beneath the Bowland shale 

Formation, Craven Group. 

Thickness 

The thickness of the formation ranges from about 220 m 

south of the middle Craven Fault, to about 140 m north of 

the North Craven Fault. 

Distribution 

southern part of the Askrigg Block, north of settle [sd 77 

to 97]. 

Age 

Holkerian to Asbian 


see also Appendix 1. members of the malham Formation in 


6.6.17.1 Cove liMesTone MeMBer (Cvls) 

Name 

see Arthurton et al. (1988); mundy and Arthurton (1980). 

malham Cove [sd 8975 6411] occurs in yorkshire near the 

village of malham, east of settle. 

Lithology 

pale grey to very pale grey limestone, mainly medium- 

and coarse-grained calcarenite, bioclastic and peloidal 

packstones and grainstones, massive to weakly bedded. 

subordinate micrites (‘porcellaneous Bed’), variably 

fenestral, and clay beds occur locally, the latter occurring in 

places above palaeokarstic surfaces. The member generally 

produces a topography characterised by steep grassy slopes, 

although the uppermost 6 m forms a continuous scar, 

commonly with an overhang. 

Stratotype 

partial type section occurs at malham Cove [sd 8975 

6411] where 72 m of the upper part of the Cove limestone 

member, including the top, is present (see Arthurton et al., 

1988). 


The lower boundary is drawn at the base of the pale grey 

limestone of the Cove limestone member where it rests 

105 

conformably (but gradationally and slightly diachronously) 

on the mid–dark grey limestone of the scaleber Quarry 

limestone member, Kilnsey Formation (Figure 15, 

Column 6), or locally, unconformably on lower palaeozoic 

strata, for example, at Crummack dale [sd 781 707 to 767 

710]. 

The upper boundary of the member is taken at a conspicuous 

bedding plane at the base of the scar-forming, pale 

grey limestones of the Gordale limestone member. 

Thickness 

some 72 m thick in its type section at malham Cove [sd 

8975 6411], and 114 m thick in the Cominco Borehole s2 

(BGs Registration Number sd86sw/6) [sd 8491 6345], 

south of the middle Craven Fault. 

Distribution 


to 97]. 


Holkerian. The macrofauna of the Cove limestone member 

is poor, though diagnostic Holkerian foraminifers occur. 

6.6.17.2 gorDale liMesTone MeMBer (gDll) 

Name 

The member is named from the limestone at Gordale scar 

[sd 913 640] (see Arthurton et al., 1988; mundy and 

Arthurton, 1980). 

Lithology 

scar-forming, mid–pale to very pale grey limestone, well 

bedded, varying from thick- to very thick-bedded. variations 

include fine- and medium-grained (more rarely coarsegrained) 

bioclastic calcarenite packstones, wackestones and 

subordinate grainstones, with thin conglomerates adjacent to 

the middle Craven Fault. The wackestones and packstones 

commonly show pseudobrecciation and the grainstones 

are cross-bedded. undulating palaeokarstic surfaces are 

present, commonly overlain by thin clays (bentonites). 

Topographically, the member forms conspicuous stepped 

scar-features and prominent limestone pavements. 

Stratotype 

The type section is at Gordale scar [sd 913 640] where 

the complete thickness (94 m) of the Gordale limestone 

member, including top and base is seen (see Arthurton et 

al., 1988). 


The lower boundary is taken at a conspicuous bedding 

plane at the base of the scar-forming pale grey, wellbedded 

limestone of the Gordale limestone member above 

the pale grey massive limestone of the Cove limestone 

member. 

The conformable upper boundary is drawn at the upward 

passage from pale grey limestone of the Gordale limestone 

member to darker grey limestone of the lower Hawes 

limestone at the base of the Alston Formation, yoredale 

Group (Figure 15, Column 6). 

Thickness 

some 94 m in its type section at Gordale scar [sd 913 640]. 

elsewhere a thickness of 70–75 m is typical. 

Distribution 


to sd 97]. 




Asbian. Typical Asbian fossils in the Gordale limestone 

member include Dibunophyllum bourtonense, Davidsonina 

septosa and Delepinea comoides. diagnostic foraminifers 

also occur. 

6.6.18 Cracoe Limestone Formation (CCOE) 

Name 

Cracoe village, after which the formation is named, 

is situated 5.5 miles north-north-west of skipton. The 

formation was previously known as the ‘marginal Reef 

limestones’ (see Arthurton et al., 1988, and references 

therein). 

Lithology 

The formation includes mid and mid–pale grey limestones 

ranging from organic boundstones to packstones and 

wackestones with a variable grainsize depending on the 

bioclastic components. Zones of megabrecciation and 

neptunian dykes (crinoid- and mudstone-filled) are present 

within the formation at its partial type section at swinden 

Quarry (see below). 


Apron reef. 

Stratotype 

A partial type section is at swinden Quarry [sd 975 

611 to 982 619], near Cracoe, North yorkshire, where a 

large carbonate bank (‘reef’) of pale grey and very pale 

grey wackestones is exposed, faulted against ‘pre-reef’ 

and ‘post-reef’ limestones. Zones of megabrecciation and 

neptunian dykes are also present in the quarry (Arthurton et 

al., 1988; see also mundy, 2000). 


south of the middle Craven Fault, occurring in a roughly 

west–east tract extending 20 km east from settle [sd 83 

63] to Burnsall [se 01 61]. The apron reef has become 

dislocated into fault-slices along the Craven Fault system. 

The formation passes northwards into the Cove limestone 

and Gordale limestone members and probably also into 

the lower Hawes limestone (Alston Formation, yoredale 

Group). 


The lower boundary has not been proved, but is likely 

to comprise reef limestones of the Cracoe limestone 

Formation resting upon the bedded, mid to mid–dark grey 

limestone of the scaleber Quarry limestone member. 

The upper boundary is a marked unconformity, with 

the reef limestones of the Cracoe limestone Formation 

overlain by dark grey mudstones of the Bowland shale 

Formation. pre-reef and post-reef limestones are present 

in the partial type section at swinden Quarry (see above), 

but the contacts with the reef limestones of the Cracoe 

limestone Formation are faulted. 

Thickness 

The total thickness has not been proved, but is in excess of 

100 m at the type locality. 


?Holkerian to Brigantian. The biota is diverse with 

biostratigraphically significant ammonoids including 

Goniatites hudsoni, G. wedberensis, Bollandites castletonensis 

and G. moorei of B 2 age (Arthurton et al., 1988), and 



106 

foraminifers of p 1a age including stellate archaediscids and 

Howchinia bradyana (strank in Arthurton et al., 1988). 

SOUTH CUMBRIA (Figure 9, Column 14) 

6.6.19 Martin Limestone Formation (MTL) 

Name 

The name is derived from martin Quarry, dalton-in- 

Furness. The martin limestone of Rose and dunham (1977) 

was given formational status by Johnson et al. (2001). 

Lithology 

The martin limestone Formation comprises grey or 

greenish grey carbonate mudstones (commonly with 

fenestrae), pelletoid and bioclastic grainstones (locally with 

small oncoliths) and ooidal limestones. The limestone is 

extensively dolomitised locally, and there is a calcareous 

or dolomitic nodular band with algal structures at the base 

(Johnson et al., 2001; Rose and dunham, 1977). 


The formation was deposited in a carbonate-dominated, 

nearshore to peritidal, restricted marine environment, 

with barrier beach complexes, tidal flats and restricted 

lagoons (Johnson et al., 2001). A more open marine 

platform carbonate facies developed in the upper part of the 

succession (Rose and dunham, 1977). 

Stratotype 

The type section is at the partly filled in martin (now 

marton) Quarry [sd 2434 7688] near dalton-in-Furness. 

leviston (1979, p. 12, fig. 2) referred to 14 m of bioclastic 

calcite mudstone with common micaceous shales and a welldeveloped 

oncolitic limestone being present 5 m above the 

base. A reference section is at meathop Quarry [sd 4316 

7928], Grange-over-sands. leviston (1979, p. 8–10, fig. 2) 

referred to about 4.5 m of dolomitised bioclastic limestone 

with interbedded grey micaceous shale and common algal 

beds, being overlain by 21.7 m of slightly dolomitised pelletic 

bioclastic limestone with common beds of black micaceous 

shale and common dolomitised stromatolitic limestone, 

beneath 19.5 m of bioclastic limestone (a higher proportion 

being highly dolomitised) without shale beds. A further 

reference section occurs in the Kendal Quarry Borehole (BGs 

Registration Number sd59sw/25) [sd 5022 9250] at Kendal 

from 84.8 to 159.75 m depth. Here, 29.14 m of limestone 

with sporadic corals overlie 27.51 m of dolomitised limestone 

and 12.3 m of dolostone with interbedded siltstone. 6 m of 

siltstone with beds of dolostone occur at the base. 


The base of the formation in Furness (south Cumbria) 

is not exposed, but it is taken to overlie the marsett 

Formation (Ravenstonedale Group) (Figure 9, Column 

14) where limestone becomes dominant over shale (Rose 

and dunham, 1977, p. 28). in practice, the base is taken in 

boreholes at the first significant shale parting. 

The upper boundary of the formation is a non-sequence 

below the grainstones of the Red Hill limestone Formation, 

the base of which may be marked by the ‘Algal Band’ of 

Rose and dunham (1977). 

Thickness 

The formation is 25–135 m thick in Furness. The variable 

thickness is attributed to onlap on to irregular ridges in the 

early palaeozoic basement topography (see Johnson et al., 

2001, p. 58).


south Cumbria and north lancashire, including the Furness 

and Cartmel, Kendal, Arnside, Carnforth and Kirkby 

lonsdale areas, separated from the stainmore Trough 

by the Howgills ‘axis’. in west Cumbria a 6–12 m thick 

shallow marine succession proved in boreholes at sellafield 

was assigned to the martin limestone Formation by 

Barclay et al. (1994) and Akhurst et al. (1997). This may 

prove unwarranted if the succession is later considered 

to be part of the marsett Formation. in the Kendal area, 

there is a transitional passage from conglomerate and 

shale of the marsett Formation (which in the stainmore 

Trough is of a mostly fluvial but locally reworked shallow 

marginal marine facies), to the lower part of what is 

considered to be a local equivalent of the martin limestone 

Formation (of carbonate-dominated, near shore to peritidal, 

restricted marine facies). The inclusion of interbedded 

fluvial facies in the lower part of the martin limestone 

Formation, suggests that the formation is more typical of 

the Ravenstonedale Group of continental and peritidal 

facies, and this appears to be further supported by the 

striking similarity noted in field characteristics between the 

lower part of the martin limestone Formation and the stone 

Gill limestone Formation. However, the upper part of the 

martin limestone Formation, at Kendal and elsewhere, 

contains a more open marine platform and ramp carbonates 

facies, typical of the Great scar limestone Group. 


Tournaisian to late Chadian. Fossils, which are more 

numerous in the upper part of the formation, include 

the coral Dorlodotia pseudovermiculare and foraminifer 

Eoparastaffella sp. (Eoparastaffella Cf4 Zone). 

6.6.20 Red Hill Limestone Formation (RHO) 

Name 

The name is derived from Red Hills Quarry, millom, southwest 

Cumbria. The Red Hill oolite of Rose and dunham 

(1977) was given formational status by Johnson et al. (2001). 

Lithology 

The Red Hill limestone Formation comprises pale grey, 

closely jointed, coarse-grained, intraclastic peloidal 

grainstone, which is cross-bedded in part. Rubbly textured 

limestone with probable nodular calcrete (the ‘Algal Band’ 

of Rose and dunham, 1977) marks the base of this unit. 


Transgressive shallow marine carbonate. 

Stratotype 

The original type section at Red Hills Quarry [sd 178 

793], millom includes 20 m of massive or poorly bedded, 

bioclastic limestone but the section is now largely obscured 

(see Rose and dunham, 1977, p. 40). Reference sections exist 

at dunnerholme [sd 2128 7963] where 21 m of the base and 

lower parts of the formation are present as pale grey, ‘oolitic’ 

and fragmental limestones with some beds being secondarily 

dolomitised (Rose and dunham, 1977, p. 41; Johnson et al., 

2001, p. 59), and meathop Quarry [sd 4316 7928], Grangeover-sands 

where the base of the formation is taken at a 

sharp, erosional contact with the subjacent martin limestone 

Formation (Johnson et al., 2001, p. 59). 


The base of the formation is a non-sequence. The lower 

boundary is taken at the base of the ‘Algal Band’ of Rose 

107 

and dunham (1977) in the type locality and elsewhere, or at 

upward change from the carbonate mudstones, grainstones 

and fine oolites of the martin limestone Formation to 

coarse grainstone (Figure 9, Column 14). 

The conformable upper boundary of the formation is 

the base of the overlying dark grey crinoidal packstones 

with conspicuous thin siltstone interbeds of the dalton 

Formation. 

Thickness 

The formation is up to about 60 m thick. 


south Cumbria. 


early Arundian. Fossils are not common, but include 

the corals Koninckophyllum sp., Michelinia megastoma 

and Palaeosmilia murchisoni. The base of the formation 

is coincident with the Arundian/Chadian boundary. The 

formation corresponds to the ‘Camarophoria isorhyncha’ 

subzone of Garwood (1913). 

6.6.21 Dalton Formation (DLB) 

Name 

The formation is named after dalton-in-Furness, Cumbria. 

The dalton Beds of Rose and dunham (1977) were given 

formational status by Johnson et al. (2001). Three informal 

divisions correspond approximately to Garwood’s (1913) 

‘Chonetes carinata subzone’, ‘Clisiophyllum multiseptatum 

Band’, and ‘Gastropod Beds’, in ascending order. 

Lithology 

The dalton Formation comprises dark grey, well-bedded, 

bituminous, crinoidal packstone with conspicuous thin 

siltstone interbeds. Three informal divisions are recognised: 

a lower division with small ‘reefs’; a middle division with 

many marine mudstone and siltstone interbeds; and an upper 

division comprising pale grey packstone and grainstone. 


The middle division of the formation was deposited in 

deeper water than the lower and upper divisions. A siltstone 

bed occurring at the base of the type section marks the 

abrupt change from shallow to relatively deeper water 

limestone deposition. 

Stratotype 

The type section of the formation is the dalton-in-Furness 

bypass (A590) road cutting from [sd 2245 7489] (base) 

to [sd 2175 7466] where a dark grey siltstone with thin 

limestone interbeds at its base is overlain by three informal 

divisions comprising mid to dark grey planar-bedded 

packstone with thin siltstone partings and reefs (lowest), 

limestone with conspicuous siltstone partings (middle), and 

bioclastic packstones and grainstones (upper). A thinner 

reference section is available in the plumpton Quarries from 

[sd 3079 7856] (base) to [sd 3106 7814]. see Johnson et 

al. (2001, pp. 59–60). 


The base of the formation is defined at the type section 

(and inferred to be the same over a wide area) at the base of 

a 1.5 m thick dark grey siltstone with limestone interbeds, 

conformably overlying bioturbated crinoidal grainstones 

of the Red Hill limestone Formation. in general, however, 

the base of the formation is taken at the first appearance 



of dark grey limestone above the pale grey fragmental 

limestones of the Red Hill limestone Formation (Figure 9, 

Column 14). 

At the upper boundary of the formation, a non-sequence 

preceded deposition of the overlying pale grey limestones 

of the park limestone Formation. 

Thickness 

The formation is about 240 m thick in low Furness, but it is 

believed to thin rapidly south and east of ulverston. 


south Cumbria, north lancashire 


Arundian. Fossils are relatively common within the 

formation and include Haplolasma subibicinum, 

Clisiophyllum multiseptatum and Michelinia megastoma. 

The characteristic Arundian brachiopod Delepinea carinata 

occurs at the base, whilst the upper part of the formation has 

the first appearance of Siphonodendron martini. 

6.6.22 Park Limestone Formation (PKL) 

Name 

The name is derived from park sop (hematite mine) [sd 

213 754] in low Furness. The park limestone of Rose 

and dunham (1977) was given formational status by 

Johnson et al. (2001). it is equivalent to Garwood’s (1913) 

‘Nematophyllum (Lithostrotion) minus subzone’. 

Lithology 

The park limestone Formation consists of pale grey or 

cream, weakly bedded, closely jointed, poorly sorted and 

bioturbated, packstone and grainstone. 


shallow marine carbonate. 

Stratotype 

The type area is the south Cumbria– Furness area. Reference 

sections are at Barker scar [sd 3330 7827] to Capes Head 

[sd 334 778] (including the crag forming the western 

boundary of old park wood), and a disused quarry at 

Ravensbarrow point [sd 3380 7749]. At Barker scar, 

the basal 45 m of the formation, and the contact with 

the underlying dalton Formation are exposed. At Crown 

Quarry at about [sd 246 728] and devonshire Quarry 

[sd 249 728] more than 150 m of limestone is exposed, 

comprising approximately the upper half of the park 

limestone and much of the urswick limestone formations 

(see Rose and dunham, 1977, pp. 35, 48–49). 


The base of the formation conformably overlies the 

dalton Formation (Figure 9, Column 14), and the absence 

of Garwood’s (1913) ‘Cyrtina carbonaria subzone’ 

suggests basal onlap. The upward change from dark grey, 

bedded packstones of the dalton Formation to pale grey, 

unbedded grainstones of the park limestone Formation 

can extend over 1 or 2 m but more generally it is even 

sharper. 

The top of the park limestone Formation is a welldeveloped 

palaeokarstic surface, locally with clay-filled 

potholes. This upper boundary shows change from typical 

park limestone to pale grey, thickly bedded, ‘pseudobrecciated’ 

limestone of the overlying urswick limestone 

Formation. 



108 

Thickness 

The formation maintains a nearly constant thickness of 

about 125 m throughout its outcrop. 


south Cumbria. The formation extends from around daltonin-Furness 

in the west, to near Carnforth in the east. 


Fossils are uncommon, but include Diphyphyllum smithi, 

Lithostrotion minus, Linoprotonia ashfellensis and 

L. corrugatohemispherica, all of which are restricted to the 

unit in the south Cumbria area. The formation almost equates 

to the Holkerian stage. The lower lithostratigraphical 

boundary seen in the Holkerian stratotype at Barker scar 

[sd 3330 7827] (George et al., 1976) is 4.2 m lower than 

the Holkerian/Arundian stage boundary (see Johnson et 

al., 2001, pp. 60–61). it should be noted that Riley (1993) 

stated that it seems likely that a considerable non-sequence 

is developed at Barker scar and that the stratotype will 

require relocation. 

6.6.23 Urswick Limestone Formation (UL) 

Name 

The name was derived from outcrops around the villages 

of Great and little urswick, low Furness. The urswick 

limestone of Rose and dunham (1977) was given 

formational status by Johnson et al. (2001). 

Lithology 

The urswick limestone Formation is wholly dominated 

by rhythmically bedded, pale grey, commonly 

‘pseudobrecciated’, biocalcarenite with stylolitic partings 

and palaeokarstic surfaces at cycle tops overlain by thin, 

bentonitic mudstone beds. it creates typical stepped karst 

scenery with griked surfaces throughout the south Cumbria 

district. A 4 m-thick bed of black mudstone with thin 

limestone interbeds, called the woodbine shale, occurs 

about 30 m above the base and splits the formation into 

informal lower and upper divisions (Horbury, 1987). 


shallow marine carbonate (emergent at times). 

Stratotype 

A nearly complete type section through the formation is 

preserved at Trowbarrow Quarry [sd 481 758]. other 

reference sections include those at the stainton Quarry 

complex (now partly obscured) from about [sd 245 

728 to 249 728], Headhouse Quarry [sd 3990 8185], 

Ravensbarrow point Quarry [sd 3380 7749], Allithwaite 

Quarry [sd 391 767], and Humphrey Head point [sd 3927 

7334 to 3929 3746] (see Rose and dunham, 1977; Johnson 

et al., 2001). 


The base of the formation is conformable, except in west 

Cumbria where it is disconformable. The lower boundary 

is at the point where the poorly bedded limestones of the 

park limestone Formation pass upwards into well-bedded 

‘pseudobrecciated’ limestones of the urswick limestone 


The upper boundary of the formation is taken where 

the predominantly pale grey, thickly bedded urswick 

limestone Formation passes upward into the predominantly 

dark grey, thinner-bedded limestones of the Alston 

Formation, yoredale Group.

Thickness 

The formation is 120–160 m thick in Furness, and 40–180 m 

thick in west Cumbria. 


south and west Cumbria to north lancashire, from the 

duddon estuary to the Carnforth area. 


Asbian. The formation corresponds almost exactly to 

the ‘Lower Dibunophyllum subzone’ (uppermost 

Holkerian to lowest Brigantian) of Garwood (1913). 

Fossils are relatively prolific and include Dibunophyllum 

bourtonense, Lithostrotion spp., Palaeosmilia murchisoni, 

Siphonodendron spp., Gigantoproductus maximus, and, 

towards the top of the unit, Davidsonina septosa. 

NORTH AND WEST CUMBRIA (Figure 9, Column 13; 

Figure 14, Columns 1, 2): 

6.6.24 Frizington Limestone Formation (FRLI) 

Name 

The name is derived from Frizington parks Quarry, 

west Cumbria. Barclay et al. (1994) proposed the name 

Frizington limestone for the exposed correlative, the 

seventh limestone (eastwood et al., 1931; Arthurton and 

wadge, 1981). Akhurst et al. (1997) treated the Frizington 

limestone with formational status. 

Lithology 

in west Cumbria the Frizington limestone Formation 

consists of thin- to thick-bedded tabular limestones with 

thin shale interbeds (Barclay et al., 1994). The lower part of 

the formation displays intensely bioturbated, mainly thin- to 

medium-bedded, sandy and silty limestone with rhizoliths, 

fenestral lime mudstones and tabular to hummocky crossbedded 

sandstones. This is overlain by a foraminiferal-rich, 

mainly medium- to thick-bedded, bioclastic packstone 

and grainstone with abundant micritised peloids, common 

lithostrotionoid sheets, and thin shale and sandy limestone 

beds. palaeokarst surfaces and calcrete and mudstone 

palaeosols are present within the upper part of the formation. 


The lower part of the formation was deposited within a 

peritidal environment; the overlying beds were deposited in 

a shallow marine setting with periodic emergence. 

Stratotype 

The sellafield 3 Borehole (BGs Registration Number 

Ny00sw/35) [Ny 02596 02646] between 1515.75 and 

1615.45 m depth below the rotary table provides a partial type 

section (including the base) comprising mostly bioclastic 

packstones, with lesser grainstones, sandy limestones at 

some levels and some thin sandstones. A few fenestral lime 

mudstones occur, mostly towards the base of the formation 

(see Barclay et al., 1994). A reference section is at 

Frizington parks Quarry (disused), west Cumbria [Ny 0405 

1560] where about 26 m of the lower part of the formation 

are seen, though not the base, which is thought to be within 

10 m of the lowest beds seen. The simplified sequence 

comprises a lower part about 9 m thick of bioclastic sandy 

limestones interbedded with packstones and grainstones, a 

middle portion about 12 m thick of mainly grainstones with 

brachiopod ‘hashes’ and coral horizons, and an upper part, 

poorly exposed, about 5 m thick of sandstones and thin 

shales (see Barclay et al., 1994). 

109 


in north and west Cumbria the base of the formation, which 

is marked locally by conglomeratic sandstone, rests either 

disconformably on the martin limestone Formation (with 

Arundian strata missing), or directly on the conglomerates 

of the Courceyan marsett Formation and lavas of the 

Cockermouth volcanic Formation (Figure 9, Column 13; 

Figure 14, Columns 1, 2). locally, the formation may 

directly overlie lower palaeozoic rocks. 

in north Cumbria the top of the formation is taken immediately 

beneath the ‘sixth shale’, which comprises the base 

of the sixth limestone unit, eskett limestone Formation. 

in the uldale area [Ny 2560 3700] the top is a palaeosol 

containing a thin coal seam (eastwood et al., 1968). in west 

Cumbria, calcretes, palaeokarst surfaces and terrigenous 

deposits are evidence of emergence and subaerial exposure 

at the top of the formation beneath the urswick limestone 

Formation. Here, early Asbian strata are missing. 

Thickness 

The formation is 50–100 m thick in west Cumbria. 


The formation occurs in west and north Cumbria between 

whitehaven and penrith. The western limit is truncated 

below the permo–Triassic basal unconformity. The eastern 

limit is taken at the Kirk Rigg Fault, along the line of the 

A66 highway, west of penrith (mcCormac, 2001). 


Holkerian. The presence of foraminifer Pojarkovella nibelis 

in the sellafield boreholes (Barclay et al., 1994) is indicative 

of the Cf5 Zone. The palaeokarst surfaces and calcrete and 

mudstone palaeosols present within the upper part of the 

formation indicate that periodic emergence preceded a 

period of nondeposition during late Holkerian and early 

Asbian times. 

6.6.25 Eskett Limestone Formation (ESKT) 

Name 

The name is newly erected for individually named units, 

or sets of units in north and west Cumbria (see Akhurst 

et al., 1997), that represent minor transgression/regression 

carbonate cyclothems (see stabbins, 1969) separated by 

emersion surfaces and palaeosols. 

Lithology 

The eskett limestone Formation is dominated by pale to dark 

grey limestones with subordinate, commonly bentonitic, 

and pale grey to buff, fine- to medium-grained micaceous 

and cross-bedded sandstone. There is also interbedded 

limestone and mudstone, black shale, siltstone, and seatearth 

that can include crinoidal and shelly fossils or plant 

remains. Historically, the lithostratigraphical succession has 

been divided into individually named units, or sets of units 

(see eastwood et al., 1931; eastwood et al., 1968; Akhurst 

et al., 1997) that represent minor transgression–regression 

carbonate cyclothems (see stabbins, 1969) separated by 

emersion surfaces and palaeosols. The names of these 

local units, in ascending stratigraphical order, are: ‘sixth 

limestone’ (including the ‘sixth shale’); ‘Fifth shale’; 

‘Fifth limestone’; ‘Fourth shale’; ‘Fourth limestone’; 

‘Third shale’; ‘Third limestone’; ‘orebank sandstone’ (or 

‘second shale’); ‘second limestone’; ‘First shale’; ‘First 

limestone’. The middle part of the succession, the ‘Fourth 

limestone’, includes limestones with prominent palaeokarst 

surfaces and distinctive fossils, which can characterise 



various fossil-rich beds (for example the Girvanella and 

Orionastrea beds and the Junceum limestone). 


A platform carbonate facies with minor marine 

transgression–regression and emergence. 

Stratotype 

The type section is eskett Quarry [Ny 0534 1673], 

Frizington, Cumbria which exposes from the Rough to the 

Junceum limestones and includes the orionastrea Band, 

and the Ethrospongia Band at the base of the Junceum 

limestone (eastwood et al., 1931, pp. 88–89). Reference 

sections include: stockhow Hall Quarry [Ny 0665 1755] 

(sixth limestone and Fifth shale); Clints Quarry [Ny 0080 

1240] (Fourth shale and Fourth limestone); and a quarry at 

Tendley Hill [Ny 088 286] (First limestone). 


The base of the formation is taken at the base of the sixth 

limestone unit (Figure 14, Columns 1, 2). This is at a level, 

which may only be defined in borehole logs, as there are 

no known surface exposures. Barclay et al. (1994) located 

the top of the underlying Frizington limestone Formation 

in a borehole at sellafield on the perceived late Holkerian/ 

Asbian boundary. However, they were unable to draw a 

correlation with the west Cumbria outcrop. 

The top of the formation, in the egremont–whitehaven– 

maryport–Cockermouth area, is marked by the cessation 

of continuous limestone deposition at the top of the First 

limestone, which is conformably overlain by the mostly 

clastic marine and deltaic facies of the stainmore Formation 

(yoredale Group). Here, at outcrop, this overlying formation 

is generally represented by the coarse-grained, fluvial 

Hensingham Grit, with a basal mudstone. immediately 

west of the Bothel Fault, the upper boundary of the eskett 

limestone Formation occurs at the top of the limestones 

with palaeokarst surfaces and distinctive fossils, the Fourth 

limestone, which is overlain by the Alston Formation 

(yoredale Group) (Figure 9, Column 13) with cyclical 

sequences of coarsening upwards sedimentary rocks including 

relatively thick and common limestones. east of the 

Bothel Fault, however, the top of the eskett limestone 

Formation is close below the Asbian–Brigantian boundary, 

at the top of the white limestone unit, which is included 

at the base of the Fourth limestone. Here again, the Alston 

Formation, just described, overlies the boundary. it should 

be stressed that division east and west of the Bothel Fault 

is purely for ease of description. The Bothel Fault is not 

implied to have exerted any penecontemporaneous effects 

on deposition. 

Thickness 

in west Cumbria the formation is about 85 m thick. 


North and west Cumbria. The uppermost unit, the First 

limestone, is the lateral equivalent of the Great limestone 

member (Alston Formation, yoredale Group) of the Alston 

Block, and the ‘main’ (now Great) limestone member of 

the Askrigg Block. 


Holkerian to pendleian. The presence of Productus 

garwoodi in the lower part of the sixth limestone at 

Rowrah (Ramsbottom, 1955) indicates that the Holkerian/ 

Asbian boundary occurs within, and not at the base of 

the formation. in west Cumbria the platform carbonate 



110 

facies continued to dominate until the early pendleian. 

The distinctive fossils of the Fourth limestone include 

Girvanella sp., Saccamminopsis sp., Orionastrea sp. 

Siphonodendron junceum and Spirorbis sp. 

ISLE OF MAN (Figure 8, Column 8) 

6.6.26 Derbyhaven Formation (DBH) 

Name 

The name is derived from derbyhaven, south isle of man. 

see Chadwick et al. (2001); lewis (1930); dickson et al. 

(1987). 

Lithology 

The formation comprises limestone, with interbedded, 

subordinate claystone and siltstone. The limestones vary 

from packstone, to wackestone and grainstone. They are 

typically grey, bioclastic (including crinoids and corals) and 

bioturbated. sedimentary structures vary but include crossbedding, 

wave ripples and hummocky cross-bedding. The 

claystones and siltstones are grey, bioclastic, and form thin, 

discontinuous beds. The formation includes three members, 

the Turkeyland, sandwick (isle of man), and skillicore 

members. 


The sequence is interpreted as representing a carbonate 

ramp facies. 

Stratotype 

dickson et al. (1987; see also Chadwick et al., 2001) 

compiled the type section from the constituent members 

along the eastern coastline of the isle of man. They 

referred to exposures of the Turkeyland member 16.7 m 

thick at derbyhaven [sC 289 678], where dolomitisation 

has destroyed much of the primary rock fabric; exposures 

of the sandwick (isle of man) member, apparently 46 m 

thick at sandwick Bay [sC 282 671], and on the foreshore 

east of Ronaldsway Airport [sC 294 684], where there 

are limestones with shale partings; and exposures of the 

skillicore member, 21 m thick on the foreshore north-east 

of the airport [sC 292 682] comprising mainly argillaceous 

limestones with abundant shale intercalations. 


The base of the formation (taken at the base of the typically 

ooidal and bioclastic grainstones of the Turkeyland member) 

is poorly defined. it rests directly on conglomerates of 

the langness Conglomerate Formation, Ravenstonedale 

Group, on the foreshore at derbyhaven [sC 2820 6607] 

(Figure 8, Column 8), although outcrops are discontinuous 

and poorly exposed. it was formerly exposed at the now 

infilled Turkeyland Quarry [sC 2950 6940], where it rests 

directly on conglomerates of the langness Conglomerate 

Formation. 

The top of the formation is poorly defined. it is overlain 

by the limestones with interbedded subordinate claystone 

of the Knockrushen Formation, with the boundary taken 

immediately above a byozoan bed, which is exposed to the 

north-east of the airport light gantry at Ronaldsway at about 

[sC 28 68], at port st mary at about [sC 21 67], and at 

Ballasalla at about [sC 28 70] (see dickson et al., 1987 who 

quoted no grid references for these localities). 

Thickness 

The formation is more than 90 m thick (Chadwick et al., 

2001).


The southern part of the isle of man, in the Castletown area. 


Arundian. The skillicore member includes the coral 

Michelinia megastoma. 


see also Appendix 1. members of the derbyhaven Formation 


6.6.26.1 TurKeylanD MeMBer (TurK) 

Name 

The Turkeyland member was named and defined by 

dickson et al. (1987). see also lamplugh (1903). 

Lithology 

limestone, typically an ooidal and bioclastic grainstone, 

dolomitic, grey, stylolitic, well-sorted, fossiliferous, with 

relict cross-bedding, wave ripples and hummocky crossbedding 

and rare claystone partings. 


The unit is interpreted as a transgressive, high energy, 

shallow marine facies deposited on a carbonate ramp. 

Stratotype 

A partial type section occurs in natural foreshore exposures 

between derbyhaven and langness point [sC 2804 6595 to 

2849 6672]: specifically 1 km north-east of langness point, 

at a point marked on the 1:50 000 scale ordnance survey 

map as Creg inneen Thalleyr [sC 281 659]. These represent 

discontinuous exposures through the entire thickness of the 

member (see Chadwick et al., 2001). 


The base of the Turkeyland member is poorly defined. it 

rests directly on sandstones of the langness Conglomerate 

Formation on the foreshore of the langness peninsula [sC 

2820 6607], although exposures are discontinuous and 

poorly exposed. it was formerly exposed at the now infilled 

Turkeyland Quarry [sC 2950 6940], where dickson et al. 

(1987) recorded it resting directly on conglomerates of the 

langness Conglomerate Formation. 

The top of the Turkeyland member is poorly exposed 

on the foreshore at derbyhaven [sC 2835 6653] where it 

is overlain by the sandwick (isle of man) member of the 

derbyhaven Formation. The boundary is gradational, taken 

at the change from limestone to limestone with interbedded 

claystones. 

Thickness 



The member occurs in the southern part of the isle of 

man, to the south-east of Castletown, from derbyhaven 

[sC 2907 6806] to Creg inneen Thalleyr [sC 2804 6595]. 

visean rocks in the northern part of the island are entirely 

concealed and it is not known whether it is present there. 

Age 

Arundian. 

6.6.26.2 sanDwiCK (isle oF Man) MeMBer (swiK) 

Name 

dickson et al. (1987) divided the singular sandwick 

member (as defined by Chadwick et al., 2001) into a 

111 

lower unit, the ‘sandwick member’, and an upper unit, the 

‘Ronaldsway member’. see also lamplugh (1903). The 

epithet (isle of man) is added to distinguish the sandwick 

(isle of man) member from the sandwick Fish Bed 

member (orkney). 

Lithology 

limestone, with interbedded subordinate claystone and 

siltstone. The limestones are packstone and wackestone, 

grey, bioclastic (including crinoids and corals), bioturbated, 

sharp based, graded beds with hummocky cross-bedding. 

The grey, bioclastic claystones and siltstones form thin, 

discontinuous beds. 


The member is interpreted as a mid-ramp carbonate facies 

with storm deposit limestones, and quiet water mudstones. 

it represents a period of maximum flooding. 

Stratotype 

A partial type section occurs in natural foreshore exposures 

700 m to the south-south-east of derbyhaven [sC 2827 

6699]. discontinuous poorly exposed outcrops are present 

through the lower half of the member [sC 2831 6718 to 

2825 6669] (see dickson et al., 1987). A reference section 

is provided on the foreshore east of Ronaldsway Farm [sC 

2924 6822 to 2941 6859]. Here about 24 m of discontinuous 

exposures in the lower part of the sandwick (isle of man) 

member are present (see dickson et al., 1987). 


The base of the sandwick (isle of man) member is poorly 

defined. it is poorly exposed on the foreshore at derbyhaven 

[sC 2835 6653] where it overlies the Turkeyland member. 

The boundary is gradational, taken at the change from 

limestone to limestone with interbedded claystones. 

The top of the member is also poorly defined as it is 

overlain by limestones, sandstones and siltstones of the 

skillicore member, with a gradational contact. it is taken 

at the appearance and increasing occurrence of fine-grained 

sandstone, together with an increase in siltstone and a more 

tabular bedding style in the skillicore member. 

Thickness 

some 46 m. 


The member occurs in the southern part of the isle of man, 

in the area east of Castletown [sC 2970 6913 to 2822 6677]. 

visean rocks in the northern part of the island are entirely 

concealed and hence it is unknown whether it is present in 

the north. 

Age 

Arundian. 

6.6.26.3 sKilliCore MeMBer (sKil) 

Name 

derived from lough skillicore and defined by Chadwick 

et al. (2001), the member was formerly named the upper 

Michelinia Beds by lewis (1930). 

Lithology 

Argillaceous limestone, with common interbedded claystone 

and siltstone and subordinate sandstone. The limestones are 

packstone, grey, bioclastic, bioturbated and pyritic, with 

wave ripple cross-lamination. The claystones and siltstones 

are grey, forming beds up to 1 m thick. They are generally 



unfossiliferous, though some are burrowed. The sandstones 

are fine-grained, cross-laminated and wave rippled. 


The unit is interpreted as an upper-ramp, shallow-water 

carbonate facies. 

Stratotype 

A partial type section, exposing the lower part of the 

member, occurs at lough skillicore [sC 2914 6831 to 2921 

6838] in an embayment of the sea on the foreshore east of 

Ronaldsway Airport (see dickson et al., 1987). 


The base of the member is poorly defined. it overlies the 

limestones of the sandwick (isle of man) member with a 

gradational contact, taken at the appearance and increasing 

occurrence of fine-grained sandstone, together with an 

increase in siltstone and a more tabular bedding style. 

The top of the member is also poorly defined. it is overlain 

by the Knockrushen Formation, with the boundary 

taken as immediately above a bryozoan-bearing limestone 

bed, which is exposed at port st mary [sC 212 672] and 

Ballasalla [sC 276 700] (dickson et al., 1987). No thickness 

is given by dickson et al. (1987) for this bed, but the 

top surface is figured in their publication (see dickson et 

al., 1987, fig. 7). 

Thickness 



The member occurs in the southern part of the isle of man, 

in the Castletown area, from Ballasalla [sC 2857 7017] to 

derbyhaven [sC 2798 6754]. visean rocks in the northern 

part of the island are entirely concealed and hence it is 

unknown whether it is present in the north. 


Arundian. The limestones have crinoids and corals 

(including Michelinia megastoma), the claystones and 

siltstones have some Chondrites burrows. 

6.6.27 Knockrushen Formation (KNRN) 

Name 

The name is derived from Knockrushen House, south isle 

of man. see Chadwick et al. (2001); lewis (1930); dickson 

et al. (1987). 

Lithology 

The formation comprises limestone, with interbedded 

subordinate claystone and siltstone at the top. limestones 

vary from wackestone to fine-grained packstone; they are 

commonly nodular in form and argillaceous. Thin beds of 

black fissile claystone are also present. siltstone is common 

near the base of the formation. 


The succession apparently represents an onshore marine 

ramp with evidence of deposition above storm wave-base 

(see dickson et al., 1987; Chadwick et al., 2001). 

Stratotype 

A partial type section is a foreshore exposure east of 

Knockrushen House [sC 2584 6627 to 2653 6727] 

where 21 m of irregularly bedded to nodular, darkgrey, 

argillaceous spicular limestones (wackestones) are 



112 

interbedded with black, fissile shales. There is a reference 

section on the foreshore by the lime kilns at scarlett [sC 

2300 6860] where the top 6 m of the formation are exposed. 

see dickson et al. (1987). 


The formation overlies the skillicore member of the 

derbyhaven Formation (Figure 8, Column 8). The basal 

boundary is taken immediately above a bryozoan bed, 

which is exposed to the north-east of the airport light 

gantry at Ronaldsway at about [sC 28 68], at port st mary 

at about [sC 21 67], and at Ballasalla at about [sC 28 70] 

(see dickson et al., 1987 who quoted no grid references for 

these localities, so the boundary can be regarded as not well 

defined). 

The top of the formation is also poorly defined. 

The wackestones and packstones of the Knockrushen 

Formation are overlain by the massive lime mudstones 

of the Hodderense limestone Formation, Craven Group. 

dickson et al. (1987) described the base of the Hodderense 

limestone Formation as occurring close [sC 2580 6620] 

to the visitor Centre at scarlett south of the old lime kilns, 

where its base is taken at the lowest mottled horizon. This 

mottling is a result of the presence of blue or grey micrite 

nodules up to 3 cm in size. 

Thickness 

The formation is 21 m thick. 


The south isle of man, in the Castletown area. 


Holkerian. The formation contains the large caninioid 

coral Siphonophyllia benburbensis and the brachipod 

Megachonetes papilionensis. Zoophycos burrows are 

common near the base. 

6.6.28 Balladoole Formation (BOOL) 

Name 

The name is derived from Balladoole, south isle of man. 

see Chadwick et al. (2001); lewis (1930); dickson et al. 

(1987). 

Lithology 

The formation comprises limestone, with interbedded 

subordinate claystone and siltstone at the top. The limestones 

are typically grey, contain crinoids, brachiopods and corals, 

and are locally dolomitic. They vary from grainstone to 

packstone, with bioherms of wackestone. large bioherms 

have been described, up to 5 m in height and 10 m in width. 


The formation represents carbonate platform edge deposits. 

Stratotype 

A partial type section is poorly exposed along the foreshore 

adjacent to Balladoole Quarry from poyll Ritchie [sC 2400 

6810] to salt spring Cottage [sC 2440 6790]. due to faulting 

the base of the formation is not exposed at Balladoole, but 

the top of the formation is seen below salt spring Cottage 

where it comprises unbedded lime-mud mounds overlain 

by a series of well-bedded skeletal limestones, intercalated 

with soft, fissile shales (see dickson et al., 1987). 


see Figure 8, Column 8. The base of the formation is

poorly defined and thought to be diachronous. it is partly 

coeval with the Bowland shale Formation, Craven Group 

and was subsequently overstepped by it (Chadwick et al. 

2001). At sea mount [sC 2590 6990] in Castletown Bay 

the Balladoole Formation rests directly on the nodular, 

cherty wackestone with scattered thin claystone layers of 

the Hodderense limestone Formation (Craven Group). 

The top of the formation is poorly defined. The Bowland 

shale Formation oversteps the Balladoole Formation at outcrop 

in a foreshore exposure north-east of spring Cottage 

[sC 2440 6790]. Here the Balladoole Formation comprises 

unbedded lime mud mounds, and the overlying Bowland 

shale Formation comprises detrital carbonates, with interbedded 

grey mudstones and debris beds, including erosively 

based, graded packstone beds. 

Thickness 

The formation is about 90 m thick. 


The southern part of the isle of man, in the Castletown area. 

Age 

Asbian. 

6.7 YOREDALE GROUP (YORE) 

There is long established usage of the term yoredale facies, 

based upon the description of yoredale cycles as early as 

phillips (1836). The name yoredale Group now replaces the 

wensleydale Group of the Askrigg Block; the Alston Group 

of the Alston Block; and the upper Border Group, and 

lower and upper liddesdale groups of the Northumberland 

Trough (waters et al., 2007). 

The yoredale Group (mixed shelf carbonate and deltaic 

(‘Yoredale’) facies and fluviodeltaic (‘Millstone Grit’) facies) 

(Figure 7) extends across the entire Northern england 

province and comprises: 

in the Northumberland Trough and Solway Basin, the 

Tyne limestone, Alston and stainmore formations; 

in the Alston Block, Stainmore Trough and Askrigg Block, 

the Alston and stainmore formations; 

in north Cumbria, the Alston Formation; 

in south Cumbria (and north Lancashire), the Alston 

Formation; 

in west Cumbria, the stainmore Formation; 

In the north Isle of Man, a sequence similar to the Alston 

Formation, and another apparently assigned to either the 

Great scar limestone Group or yoredale Group. These 

are known only in boreholes (see Chadwick et al., 2001). 

The yoredale Group comprises repeated, typically upwardcoarsening 

cycles of basal, laterally extensive marine 

limestone, marine shale (commonly bioturbated), thin 

sandstone commonly topped with seatearth or ganister 

and an overlying coal. The limestones are typically mid to 

dark grey, thin-bedded and biomicritic, with a restricted 

benthic fauna and rare ammonoids. The sandstones are 

typically pale grey, fine- to medium-grained and quartzitic 

to subarkosic. The clastic component was deposited by progradation 

of high-constructive lobate deltas, though there 

113 

is evidence to suggest that there has been extensive shallow 

marine reworking of clastic sediments following delta 

abandonment (elliott, 1975). large fluvial channels were 

incised into underlying cyclothems on the Alston Block 

during the Brigantian and pendleian (dunham, 1990), and 

in Northumberland an element of tectonic control on this 

process can be demonstrated (young and lawrence, 2002). 

The marine limestones were deposited during sea-level 

rises and when delta lobes were switched or abandoned. 

The cycles, which range from 5–90 m thick, are named after 

the limestone present at the base of the cyclothem (leeder 

et al., 1989). limestones have bed status unless there are 

good reasons for them to have member status. minor limestones 

and sandstones remain informal beds. dunham and 

wilson (1985) provided details of limestone nomenclature 

and correlations, and cyclothem thicknesses for the Askrigg 

Block and stainmore Trough, and dunham (1990) provided 

similar information for the Alston Block. on the north isle 

of man undifferentiated strata assigned to either the Great 

scar limestone Group or the yoredale Group occurs in the 

Ballavaarkish (shellag North) Borehole [NX 4625 0070] 

between 172.34 and 179.60 m depth. They comprise massive, 

stylolitised, fractured and sucrosic dolostone, which 

may be of early Namurian or visean age, but diagenesis has 

destroyed any biostratigraphical evidence (see Chadwick et 

al. 2001). 

The conformable but diachronous base of the yoredale 

Group is typically taken at the base of marine limestone 

marker bands. in the solway Basin, Northumberland 

Trough, Cheviot Block and north-east Northumberland, the 

sandstones of the Fell sandstone Formation, Border Group 

pass upward, locally unconformably and diachronously, 

into the Tyne limestone Formation, yoredale Group; the 

lower boundary of which is variably represented as the base 

of the Clattering Band or its correlative the Kingsbridge 

limestone, or in the langholm area, the Glencartholm 

volcanic Beds. 

in the Brough-under-stainmore and penrith districts 

the Robinson limestone of the melmerby scar limestone 

Formation, Great scar limestone Group, is overlain by 

siltstone or sandstone of the Tyne limestone Formation, 

yoredale Group. There is evidence of penecontemporaneous 

erosion and potholing on the top surface of the 

Robinson limestone. 

in east Cumbria and the stainmore Trough, the lower 

boundary of the yoredale Group occurs where the top of 

the mostly thick-bedded, pale to mid grey limestone of the 

Knipe scar limestone Formation, Great scar limestone 

Group, is disconformably overlain by the variable sandstone 

and mudstone wintertarn sandstone member of the 

Tyne limestone Formation. 

on the northern Askrigg Block, the pale to mid grey 

limestones (with palaeokarst surfaces) and subordinate 

mudstones of the danny Bridge limestone Formation, 

Great scar limestone Group pass upward into the crossbedded, 

regressive sandstones of the wintertarn sandstone 

member, Tyne limestone Formation. 

in the settle area, the lower boundary of the yoredale 

Group is generally taken where the paler grey, thick- to 

very thick-bedded limestone with palaeokarst surfaces 

of the malham Formation, Great scar limestone Group 

pass upward into the darker grey lower Hawes limestone 

(Alston Formation) at the base of the yoredale facies 

sequence. 

in west Cumbria, in the egremont–whitehaven– 

maryport–Cockermouth area, the lower boundary of the 

yoredale Group occurs where the shelf carbonate sequence 

of the First limestone, eskett limestone Formation is 



terminated and conformably overlain by the mostly clastic 

marine and deltaic facies of the stainmore Formation. 

However, at outcrop the basal part of the stainmore 

Formation generally comprises the coarse-grained, fluvial, 

Hensingham Grit, with a basal mudstone. 

in north Cumbria, east of the Bothel Fault, the lower 

boundary of the yoredale Group occurs above the pale to 

dark grey limestones of the eskett limestone Formation, 

Great scar limestone Group, at the top of the white 

limestone unit, which forms the base of the Fourth 

limestone. immediately west of the Bothel Fault, however, 

the same boundary occurs at the top of the Fourth 

limestone, which is distinguished by the inclusion of palaeokarst 

surfaces and distinctive fossils. it should be stressed 

that division east and west of the Bothel Fault is purely for 

ease of description. The Bothel Fault is not implied to have 

exerted any penecontemporaneous effects on deposition. 

in south Cumbria, the lower boundary of the yoredale 

Group is at the point where the predominantly pale grey, 

thickly bedded limestones of the urswick Formation, Great 

scar limestone Group, pass up into the predominantly 

dark grey, thinner bedded limestones and mudstones of the 

Alston Formation. 

on the northern part of the isle of man, platform carbonates 

of the Balladoole Formation, Great scar limestone 

Group are thought to be overlain by a cyclothemic mixed 

carbonate clastic sequence, similar to the Alston Formation, 

yoredale Group of south Cumbria. 

The top of the yoredale Group is defined in north, 

west and east Cumbria, the solway Basin, the stainmore 

and Northumberland troughs, on the Alston Block and in 

north-east Northumberland by the base of the pennine Coal 

measures Group (fluviodeltaic (‘Coal Measures’) facies). 

To the north of wensleydale on the Askrigg Block and in 

the settle area, it is defined by the base of the millstone 

Grit Group (fluviodeltaic (‘Millstone Grit’) facies). on 

the northern part of the isle of man the top of what may 

be either the Great scar limestone Group or the yoredale 

Group is also defined by the base of the millstone Grit 

Group. in south Cumbria the base of the Craven Group 

(hemipelagic facies) defines the top of the yoredale Group. 

The type area of the yoredale Group is the valley of the 

River ure, wensleydale on the Askrigg Block (see phillips, 

1836; George et al., 1976; dunham and wilson, 1985), and 

it extends across the entire Northern england province. 

Thickness varies greatly since the group, formations and 

individual sandstones tend to thicken into troughs and halfgrabens, 

and conversely all the elements of any rhythm 

may be reduced or absent. The range in thickness is from 

50 m in the lamplugh area of west Cumbria (young and 

Bolland, 1992) to a proved maximum of 1219 m in the seal 

sands Borehole (BGs Registration Number NZ52sw/457) 

[NZ 538 238] in the eastern part of the stainmore Trough 

(dunham and wilson, 1985). in south Cumbria the group 

is 80–180 m thick, and over 500 m of strata are present 

in the solway Basin in boreholes north of maryport. on 

the Askrigg Block, generalised vertical sections on BGs 

maps suggest a range of thickness in the order of about 

200–900 m, and there are marked thickness variations 

across the stublick–Ninety Fathom Fault, separating the 

Northumberland Trough from the Alston Block, to the 

south. 

The age of the yoredale Group is Holkerian or Asbian 

to yeadonian. The base is diachronous, and ranges from 

Holkerian in the Kirkbean outlier and early Asbian in 

the Northumberland Trough and solway Basin, to early 

Brigantian on the Alston and Askrigg blocks, in the 

stainmore Trough and in south Cumbria, to pendleian in 



114 

north and west Cumbria where there is also a large nonsequence 

within the group in which strata of Chokierian to 

marsdenian age are absent (Akhurst et al., 1997). in south 

Cumbria, only the visean part of the succession is present. 

The top of the group is latest yeadonian nearly everywhere, 

the exceptions being on the Askrigg Block where 

it is late pendleian and south Cumbria where it is late 

Brigantian. in the north isle of man the top of the sequence, 

which is similar to the Alston Formation, is at least early 

Namurian, but the age of the top of what may be either 

Great scar limestone Group or yoredale Group strata at 

the base of the Ballavaarkish (shellag North) Borehole 

(see above) remains uncertain (see Chadwick et al., 2001). 

The base of the Namurian series is defined as the base 

of the Cravenoceras leion marine Band. The position of 

this marine band is taken to be near the base of the Great 

limestone member (see Johnson et al. 1962). 

6.7.1 Tyne Limestone Formation (TYLS) 

Name 

The name is derived from the River Tyne, Northumberland. 

Lithology 

in the solway Basin, the Tyne limestone Formation 

comprises a heterogeneous yoredale Group cyclicity, with 

limestone and sandstone components absent from parts 

of the succession. The sandstones tend to thicken into 

troughs and half-grabens. The formation includes the 

Glencartholm volcanic Beds at the base, which comprises 

a succession of tuffs, volcaniclastic sedimentary rocks and 

subordinate basalt lavas, 150–180 m thick (lumsden et 

al., 1967; williamson in stephenson et al., 2003). in the 

Northumberland Trough, the ‘scremerston Coal member’ 

comprises up to 300 m of shales and limestones, sandstones 

and thick coals (smith, 1967; leeder et al., 1989), and 

passes transitionally south-west into typical cyclicity. The 

Tyne limestone Formation is distinguished from the Alston 

Formation by the common presence of thick, commonly 

bioclastic limestones in the latter. 


shallow water marine and deltaic. 

Stratotype 

The partial type section is the Archerbeck Borehole (BGs 

Registration Number Ny47Nw/14) [Ny 4160 7820] from 

the base of the Cornet limestone at 504.7 m depth to 

within the Glencartholm volcanic Beds at the bottom 

of the borehole at 1403.3 m depth (see lumsden and 

wilson, 1961). Reference sections include the stonehaugh 

Borehole (BGs Registration Number Ny77Ne/2) [Ny 

7899 7619] from rockhead at about 4 m depth to the 

possible Kingbridge limestone at about 211 m depth; the 

Ridsdale Borehole (BGs Registration Number Ny88se/1) 

[Ny 8946 8288] from the Redesdale limestone at 0.91 m 

depth to strata below the lower millerhill limestone at 

305.41 m depth; the Ferneyrigg Borehole (BGs Registration 

Number Ny98se/13) [Ny 9579 8364] from the base of the 

low Tipalt limestone at 77.32 m depth to strata below the 

Furnace Coal at 457.50 m depth; the River Black lyne, 

north of dappleymoor Fault, from between dodgsonstown 

Ford [Ny 5009 7452] and the bend [Ny 4987 7511] southwest 

of Cumcrook, Bewcastle; the Cairing Croft Borehole 

(BGs Registration Number Ny66Ne/2) [Ny 6626 6700] 

from the base of the low Tipalt limestone at about 85 m 

depth to strata below the Thirlwall Coal at about 413 m 

depth; and the Hoddom No. 2 Borehole (BGs Registration

Number Ny17Ne/3) [Ny 1641 7280] between 3.2 and 

41.6 m depth. 


in the solway Basin, Northumberland Trough, Cheviot 

Block and north-east Northumberland, the sandstones of 

the Fell sandstone Formation, Border Group pass upward, 

locally unconformably and diachronously, into the Tyne 

limestone Formation, the lower boundary of which is 

variably represented as the base of the Clattering Band or its 

correlative the Kingsbridge limestone (Figure 8, Column 11; 

Figure 11, Columns 1–3), or in the langholm area, the 

Glencartholm volcanic Beds (Figure 10, Column 3). 

The upper boundary of the formation is conformable with 

the base of the Alston Formation, normally at the base of 

the low Tipalt or Callant limestone (Figure 6, Column 7; 

Figure 8, Column 11; Figure 10, Column 3; Figure 11, 

Columns 1–3). However, in districts where the formally 

defined upper boundary of the Tyne limestone Formation 

has not or cannot be mapped, at the base of the limestone 

that marks the base of the Brigantian stage, the upper boundary 

is taken at the top of the next, widely mapped limestone 

below it. This means that in the Rothbury district, for example, 

the top of the Tyne limestone Formation is taken at the 

top of the dun limestone (Figure 13, Column 3). 

Thickness 

The formation tends to thicken into troughs and halfgrabens. 

The Glencartholm volcanic Beds are 150–180 

m thick (150 m proved in the Archerbeck Borehole — see 

above; lumsden et al., 1967). The ‘scremerston Coal 

member’ is up to 300 m thick at Berwick (smith, 1967). 


solway Basin, Northumberland Trough, Cheviot Block 

north-east Northumberland, and north-west england. 


Holkerian to Asbian. The brachiopod Linoprotonia 

corrugatohemisphaerica is diagnostic of the Holkerian. 

others that also occur include Punctospirifer scabricosta 

and Composita ambigua. Corals, including Dibunophyllum 

sp., Lithostrotion portlocki and Siphonodendron martini, and 

gigantoproductoid brachiopods are common in the Asbian. 


see also Appendix 1. members of the Tyne limestone 

Formation include: 

6.7.1.1 arBiglanD liMesTone MeMBer (arlM) 

Name 

previously known as Arbigland Group (Craig, 1956) and 

Arbigland Beds (deegan, 1970). The status was changed 

from the Arbigland limestone Formation (lintern and 

Floyd, 2000) to a member of the Tyne limestone Formation. 

Lithology 

The member comprises interbedded marine limestone, 

mudstone and subsidiary siltstone, with thick cross-bedded, 

bioturbated, medium-grained sandstone. 

Stratotype 

The type section is the Arbigland coast, Kirkcudbrightshire, 

from Arbigland [NX 9940 5720] to Hogus point [NX 

9970 5880], where mudstones, siltstones, sandstones, and 

limestones constitute a section probably more than 300 m 

thick (Craig, 1956; deegan, 1970; but see lintern and 

Floyd, 2000, p. 82). 

115 


The base of the Arbigland limestone member is probably 

conformable on the Thirlstane sandstone (powillimount 

sandstone member, Fell sandstone Formation) (Figure 10; 

Column 2). it is stratigraphically the highest unit in the 

Kirkbean outlier, and its top is not exposed. 

Thickness 



The Kirkbean outlier of the Kirkcudbright — dalbeattie 

district. 


Asbian. The limestones and mudstones have an abundant and 

diverse fauna of corals (including Lithostrotion clavicatum, 

Siphonodendron scotica and Siphonophyllia benburbensis), 

brachiopods (including Actinopteria persulcata, 

Linoprotonia cf. ashfellensis, Productus cf. garwoodi, 

Punctospirifer scabricosta redesdalensis and Stenoscisma 

cf. isorhyncha), bivalves (including Prothyris cf. oblonga 

and Pteronites cf. angustatus) and other molluscs, crinoids 

and bryozoa. Siphonophyllia benburbensis is unknown in 

strata earlier than the Asbian. 

6.7.1.2 Dun liMesTone MeMBer (Dnl) 

Name 

previously referred to as the ladies wood limestone 

(obsolete) in the Bellingham district, and the lamberton 

limestone (obsolete) in the eyemouth district. see Frost 

and Holliday (1980); Greig (1988); Gunn (1900). 

Lithology 

A dark grey, argillaceous, crinoidal, shelly limestone with 

algal nodules, weathering to a rusty ochreous colour. 


of marine origin 

Stratotype 

The type area is the north side of Huds Head, spittal, near 

Berwick-upon-Tweed, Northumberland [Nu 010 510 to 

015 506] (see scrutton, 1995). 


At the lower boundary, the dun limestone is generally 

underlain conformably by a thin marine mudstone that 

overlies a thin coal or seatearth of the Tyne limestone 

Formation (Figure 12, Columns 1–4). 

The upper boundary of the member is generally a conformable 

change from limestone to overlying marine mudstone 

that passes up into deltaic arenaceous deposits of the 

Tyne limestone Formation (or Alston Formation, where the 

normal boundary at the base of the limestone that marks the 

base of the Brigantian stage has not or cannot be mapped). 

Thickness 

Between 1.2 and 1.6 m in the eyemouth and north 

Berwickshire districts. 5–8 m in Northumberland (Frost and 

Holliday 1980). 


Confined to Berwickshire and north Northumberland 

in the Tyne limestone Formation, yoredale Group, the 

dun limestone is widely correlatable throughout the 

Northumberland Trough (Frost and Holliday, 1980). The 

contained fauna and flora is equivalent to the macGregor 



marine Bands of the midland valley of scotland (wilson, 

1974; Neves et al., 1973). 


Asbian. An Nm Zone miospore assemblage was reported 

by Neves et al. (1973) in the dun limestone member 

in the marshall meadows Borehole (BGs Registration 

Number NT95Ne/5) [NT 9797 5685], and an Asbian age 

is supported by the presence of the coral Siphonodendron 

junceum (see Fowler, 1926). 

6.7.1.3 winTerTarn sanDsTone MeMBer (wTrs) 

Name 

The member was previously known as the Thorney Force 

sandstone (BGs, 1997). see Arthurton and wadge (1981); 

Burgess and Holliday (1979); mcCormac (2001), Rowley 

(1969). 

Lithology 

sandstone, with subsidiary siltstone, mudstone and 

limestone. 

Stratotype 

The type section is a borehole at Flusco limeworks (BGs 

Registration Number Ny42Ne/1) [Ny 4587 2905] from 

54.73 to 59.84 m depth with sandstone and a thin bed of 

mudstone (Arthurton and wadge, 1981, p. 153). 


The base is the top of the uppermost thick-bedded limestone 

of the Great scar limestone Group (Figure 9, Columns 16, 

17; Figure 14, Column 3; Figure 15, Column 3). it may be 

locally erosive. 

The top of the member is at the base of the overlying 

wackestones and packstones of the Askham limestone 

member, Alston Formation. 

Thickness 



North-west england. 

Age 

Asbian. 

6.7.2 Alston Formation (AG) 

Name 

The name is derived from the former Alston Group of 

the Alston Block and stainmore Trough, which formerly 

included platform carbonates as well as ‘yoredale’ facies 

(George et al., 1976). in south Cumbria the Alston Formation 

now replaces the Gleaston Formation of Rose and dunham 

(1977). in north Cumbria it includes the upper part of the 

now obsolete Chief limestone Group. 

Lithology 

The Alston Formation normally (but see below) extends 

stratigraphically from the base of the peghorn limestone 

(or correlatives) to the top of the Great limestone (or 

correlatives). The formation is distinguished from the Tyne 

limestone and stainmore formations by the common presence 

of thick, commonly bioclastic limestones. distinctive facies 

variations within the formation are recommended to be 

given member status. Numerous local names exist for the 

major limestones but their lateral persistence allows a single 

nomenclature to be applied across most of north and north- 



116 

east england. This has been standardised in the stainmore 

region and includes, in ascending stratigraphical order, 

the peghorn limestone, smiddy limestone, lower little 

limestone, Jew limestone, Tynebottom limestone, single 

post limestone, scar limestone, Five yard limestone, 

Three yard limestone, Four Fathom limestone, iron post 

limestone, and Great limestone. 

in a few areas closely spaced, and individually named, 

limestone beds may merge to give a differently named 

unit. For example, the peghorn and smiddy limestones of 

the edenside and north Cumbria districts, when combined, 

are known as the Askham limestone member. The Great 

limestone member includes the uppermost limestone of the 

formation. This was formerly known as the main limestone 

on the Askrigg Block. Throughout most of the region it 

comprises an uncharacteristically thick, bioclastic, locally 

biostromal, limestone. it has been correlated with the Top 

Hosie limestone of the midland valley of scotland, and the 

First limestone in Cumbria. 

in south Cumbria (see Rose and dunham, 1977; Johnson 

et al., 2001) the formation comprises a variable succession 

of thinly interbedded dark grey to black limestone, shaley 

mudstone and subordinate (and impersistent) sandstone. The 

limestones are richly fossiliferous in places with a coral–brachiopod 

fauna, and some beds have been linked with name 

equivalents in the Askrigg Block area suggesting depositional 

continuity. The Girvanella Nodular Band of Garwood (1913) 

occurs at or near the base of the formation in south Cumbria. 

Carboniferous rocks in the northern part of the isle of man are 

entirely concealed and poorly known, but a cyclothemic, mixed 

carbonate (grey argillaceous limestone)–clastic sequence similar 

to the Alston Formation of south Cumbria has been proved 

in boreholes (see Chadwick et al., 2001). 


The Alston Formation typically represents cycles of 

marine to fluvio-deltaic sedimentation. east of morecambe 

Bay it is poorly exposed, shows considerable structural 

complexity, and displays characteristics of deposition on 

a deeper shelf. west of morecambe Bay the cycles pass 

laterally into the hemi-pelagic succession of the Bowland 

shale Formation. 

Stratotype 

The type area of the formation is the Alston Block. it is 

proposed that the original type section in Augill Beck, 

Cumbria (see Burgess and Holliday, 1979) is replaced 

by the Rookhope Borehole (BGs Registration Number 

Ny94sw/1) [Ny 9375 4278] weardale, from rockhead in 

the upper part of the Great limestone at 6.86 m depth to 

the base of the peghorn limestone at 331.7 m depth (see 

Johnson and Nudds, 1996; Cozar and somerville, 2004). 

in south Cumbria the formation occurs in boreholes at 

Harbarrow No. 1 (BGs Registration Number sd27se/37) 

[sd 2531 7197] from 39.01 to 135.94 m depth and Gleaston 

Castle Farm (BGs Registration Number sd27se/51) [sd 

2549 7185] from 124.27 to 165.36 m depth (the bottom 

of the borehole). Natural sections in south Cumbria occur 

at Gleaston and on the east shore [sd 3906 7469] of 

Humphrey Head; the Kirkhead Railway Cutting [sd 3949 

7524]; and, most extensively, in Holker park at about [sd 

350 774] in a succession, mostly exposed, of limestones and 

sandstones with sporadic siltstone and coal some 140 m thick 

(see Johnson et al., 2001; Rose and dunham, 1977). on the 

north isle of man in the Ballaghenny Borehole of lamplugh 

(1903, pp. 286–288), cyclothemic ‘yoredale’ facies of 

mixed carbonate–clastic lithologies have been attributed to 

the yoredale Group (see Chadwick et al., 2001).


in the Northumberland Trough and solway Basin, the 

base of the Alston Formation, defined at the base of the 

peghorn limestone (or its correlatives), lies conformably 

on the Tyne limestone Formation (Figure 6, Column 7; 

Figure 8, Columns 11,12). in the Brough-under-stainmore 

and penrith districts the peghorn limestone is underlain by 

siltstone or sandstone of the wintertarn sandstone member, 

Tyne limestone Formation (Figure 9, Column 16). 

in east Cumbria and the stainmore Trough, the lower 

boundary occurs sharply at the base of the Askham 

(peghorn) limestone on the mainly sandstones of the 

wintertarn sandstone member (Figure 9, Column 16; 

Figure 14, Column 3). on the northern Askrigg Block, the 

Hawes (peghorn) limestone occurs above the cross-bedded, 

regressive sandstones of the wintertarn sandstone member, 

Tyne limestone Formation (Figure 15, Column 3). 

in north Cumbria, east of the Bothel Fault, the lower 

boundary of the Alston Formation occurs at the top of the 

white limestone unit at the base of the Fourth limestone, 

eskett limestone Formation (Great scar limestone Group) 

(Figure 14, Column 2), which comprises pale to dark grey 

limestones. immediately west of the Bothel Fault, the lower 

boundary of the Alston Formation is at the top of the limestones 

with palaeokarst surfaces and distinctive fossils, the 

Fourth limestone (Great scar limestone Group). it must be 

stressed that this division at the Bothel Fault is purely for 

ease of description. The fault is not implied to have exerted 

any penecontemporaneous effects on deposition. 

in south Cumbria the lower boundary is at the point 

where the thickly bedded pale grey limestones of the 

urswick limestone Formation, Great scar limestone 

Group, pass up into the predominantly dark grey, thinnerbedded 

limestone and mudstone of the Alston Formation 

(Figure 9, Column 14). The Girvanella Nodular Band of 

Garwood (1913) may mark the base of the formation. 

in districts where the formally defined lower boundary 

to the Alston Formation has not or cannot be mapped at the 

base of the limestone that marks the base of the Brigantian 

stage, that boundary is taken at the top of the next, widely 

mapped limestone below it. This means that in the Rothbury 

district, Northumberland Trough, for example, the base of 

the Alston Formation is taken at the base of the Asbian 

strata that overlie the dun limestone, Tyne limestone 


on the north isle of man, the platform carbonates of the 

Balladoole Formation, Great scar limestone Group, are 

thought to be overlain by a cyclothemic mixed carbonate– 

clastic sequence similar to the Alston Formation of south 

Cumbria. 

The top of the formation is generally defined by the base 

of the stainmore Formation with its cyclical succession of 

mudstones, siltstones, sandstones and thin limestones and 

thin coals. However, in south Cumbria the upper boundary 

is taken at the base of the Cravenoceras leion marine 

Band where the thinly interbedded limestones, mudstones 

and subordinate sandstones of the Alston Formation pass 

upward into the thick mudstones and fine-grained siltstones 

of the overlying Bowland shale Formation, Craven Group 


Thickness 

The formation tends to thicken into troughs and half-grabens. 

it is 80–180 m thick in south Cumbria, 200–250 m thick 

in the Appleby district, up to 300 m thick in edenside and 

about 337 m thick in the Rookhope Borehole (see above) on 

the Alston Block, and 600 m thick in the stainmore Trough. 

offshore, in the Keys embayment, between the isle of man 

117 

and the west Cumbria coast, a well proved 108 m of strata 

equated with the probable onshore Alston Formation. 


south Cumbria and north lancashire from the duddon 

estuary to the Carnforth area, the Askrigg and Alston 

blocks, the stainmore and Northumberland troughs, and the 

solway Basin. The formation also occurs in north Cumbria, 

east and immediately west of the Bothel Fault (though it is 

not implied that the fault exerted any penecontemporaneous 

effects on deposition), and apparently, on borehole evidence, 

on the north isle of man. 


Asbian in places, but generally Brigantian to pendleian. in the 

River eden [Ny 7832 0375] at Janny wood on the Alston 

Block, the peghorn (lower smiddy) limestone is defined as 

the Brigantian stage Basal stratotype (George et al., 1976). 

microfaunal dating in the Rookhope Borehole suggests mostly 

Brigantian (Cf6 subzone age), but early serpukhovian 

(pendleian) for the Great limestone member (Cozar and 

sommerville, 2004). The base of the Namurian, defined as the 

base of the Cravenoceras leion marine Band, is taken as near 

the base of the Great limestone. in south Cumbria the richly 

fossiliferous limestones commonly have various species of 

Lithostrotion and Siphonodendron, and the following corals 

and brachiopods are, according to Rose and dunham (1977), 

restricted to the formation here: Actinocyathus floriformis, 

Aulophyllum pachyendothecum, Dibunophyllum bipartitum, 

Diphyphyllum lateseptatum, Eomarginifera cambriensis, 

Productus hispidus, and Pugilis pugilis. The unit in south 

Cumbria equates with the ‘upper Dibunophyllum subzone’ of 

Garwood (1913) and is visean (Brigantian) in age. onshore, 

on the north isle of man the yoredale facies attributed to 

the Alston Formation in the Ballaghenny Borehole may be 

Namurian (or visean) in age (see Chadwick et al., 2001). 


see also Appendix 1. members of the Alston Formation in 


6.7.2.1 asKHaM liMesTone MeMBer (asKl) 

Name 

Named after the village of Askham, east Cumbria. see 

Rowley (1969), and Burgess and Holliday (1979); dunham 

(1990); Arthurton and wadge (1981); mcCormac (2001). 

Lithology 

limestone, dark grey, well-bedded, wackestone and 

packstone, porcellanous in parts. prominent layers with 

algal oncoliths and coral colonies. The member is split into 

2 leaves by a thin layer of red-brown mudstone. 

Stratotype 

The type section is an abandoned roadside (east side of minor 

road) quarry [Ny 583 171] beside wintertarn Farm, by shap, 

Cumbria (Rowley, 1969) where the limestone, a mid grey 

biomicrite, is divided into two parts by an algal horizon, 

most likely the equivalent of the Girvanella Bed of Garwood 

(1913). A reference section is the Flusco lodge disused quarry 

[Ny 474 282], 3.8 km west of the m6 penrith interchange, 

where a full section of the limestone is preserved, along with 

the top part of the underlying wintertarn sandstone member, 

Tyne limestone Formation (mcCormac, 2001). 


The base of the member is sharp, occurring at the base 

of a limestone bed overlying the mainly sandstone of the 



1 

BERWICK UPON TWEED 

AND NORHAM 


BORDER GROUP 


STAINMORE 

FORMATION 

TYNE LIMESTONE FORMATION ALSTON FORMATION 

FELL SANDSTONE FM 




LTLS 

GL 

FFL 

TYL 

EWL 

OXL 

WDEL 

DNL 

INVERCLYDE GROUP BORDER GROUP 


TYNE 

BALLAGAN FM FELL SANDSTONE FM 

LIMESTONE FM 


2 

FORD 

V 

KELSO VOLCANIC 

FORMATION 

SCALE 

150 

metres 

0 

FFL 

TYL 

EWL 

OXL 

WTLL 

WDEL 

DNL 

DDL 

CHML 


TYNE LIMESTONE FM 

118 

3 

HOLY ISLAND 

LKL 

GL 

ALSTON FORMATION STAINMORE FORMATION 

2 

1 

FFL 

TYL 

EWL 

‘Budle 

Limestone’ 

OXL 

WTLL 

WDEL 

DNL 

BORDER 

GROUP 

3 


STAINMORE FORMATION 


TYNE 

LIMESTONE FM 

4 

ALNWICK 

‘Upper Foxton 

Limestone’ 

‘Lower Foxton 

Limestone’ 


FORMATION 

LOCALITIES 

Figure 12 Northumberland Trough. Generalised vertical sections for Carboniferous strata at Berwick-upon- 

Tweed, Ford, Holy island and Alnwick. Based on iGs (1972, 1974, 1976, and 1977). The profiled location of 

the numbered sections is given in the inset map. see Appendices 1 and 2 for the names of the 

lithostratigraphical units shown by BGs lexicon of Named Rock units computer codes. v indicates named 

volcanic units; blue colour indicates named limestone beds. dashed lines indicate conjecture. 

4 

NORTH 

SEA 

N 

98001787 

SUS 

LKL 

CUL 

GREAT 

LIMESTONE 

MEMBER 

FOUR 

FATHOM 

LIMESTONE 

MEMBER 

THREE YARD 

LIMESTONE 

MEMBER? 

EELWELL 

LIMESTONE 

MEMBER 

CBLM 

OXFORD 

LIMESTONE 

MEMBER 

WDEL? 

DNL 

DDL


1 

ELDSON (W) 

TYNE LIMESTONE FORMATION ALSTON FORMATION 

BORDER FELL SANDSTONE 

GROUP FORMATION 

metres 

SCALE 

FLL 

RDL 

PCL 

PLDL 

150 

0 


2 

ELDSON (E) 


TYNE LIMESTONE FM 

BORDER FELL SANDSTONE 

GROUP FORMATION 

OXFORD 

LIMESTONE 

MEMBER 

PFLS 

FLL 

RDL 

PENNINE COAL 





BORDER GROUP 


3 

ROTHBURY 

BALLAGAN FORMATION FELL SANDSTONE FM TYNE LIMESTONE FM ALSTON FORMATION STAINMORE FORMATION 

119 

L 

PENNINE LOWER 

COAL MEASURES 

FORMATION 

M 

M 

M 

MTMB (HMMB) 

VDMB (HAMB) 

SWMB 

SBMB (QBMB) 

PILS 

‘Stanton 

Limestone’ 

BHGL 

LTLS 

GL 

FFL 

SXYL 

EWL 

? 

OXFORD 

LIMESTONE 

MEMBER 

DNL 

1 

2 



4 

MORPETH 





LOCALITIES 

M 

M 

M 

M 

M 

M 

PENNINE LOWER 

COAL MEASURES 

FORMATION 

M 

M 

M 

Figure 13 Northumberland Trough. Generalised vertical sections for Carboniferous strata at elsdon, 

Rothbury and morpeth. Based on GsGB (1951), iGs (1966), mills and Holliday (1998), young (1998), young 

and lawrence (1998) and dean (2001). The profiled location of the numbered sections is given in the inset 

map. see Appendices 1 and 2 for the names of the lithostratigraphical units shown by BGs lexicon of Named 

Rock units computer codes. m marine band; l Lingula band. Blue colour indicates named limestone beds. 

dashed lines indicate conjecture. 

3 

4 

AGMB (RYMB) 

SOMB (HYMB) 

HTMB (KMB) 

CWMB (LTMB) 

MTMB (HMMB) 

VDMB (HAMB) 

AMMB (GUMB)? 

LSMB (KLMB)? 

SBMB (QBMB) 

DTNL (STFL) 

NWL 

THL 

PHL 

CORL 

BSDL 

NWNL 

OKL 

FENL 

LTLS 

GREAT LIMESTONE 

MEMBER 

FOUR FATHOM 

LIMESTONE 

MEMBER 

THREE YARD 

LIMESTONE 

MEMBER 

RBUL, RBML, RBLL 

EELWELL 

LIMESTONE 

SWOL MEMBER 

UBWL 

NORTH 

SEA 

N 

98001788 



WARWICKSHIRE GROUP 

PENNINE COAL MEASURES 

GROUP 



YORESDALE 

GROUP 

GREAT SCAR 


ESKETT 

LIMESTONE FM 

WEST CUMBRIA 

WHITEHAVEN SANDSTONE 

FORMATION 

STAINMORE 

FORMATION 

1 

MILLYEAT 

MEMBER 

BRANSTY CLIFF 

SANDSTONE 

MEMBER 

M 

PENNINE LOWER 

COAL MEASURES 

FORMATION 

MARSETT 

FORMATION 


GROUP 

M 

M 

PENNINE UPPER 

COAL MEASURES 

FORMATION 

M 

M 

M 

M 



CAMB 

AGMB 

HTMB (BMET) 

VDMB (SWYMB) 

SBMB 

G1B1 

LM1 

LM2 

LM3 

LM4 

LM5 

LM6 

LM7 

FRIZINGTON 

LIMESTONE 

FORMATION 

LGMB 

AMMB 

LSMB 

HNMB 

FRIZINGTON 

LIMESTONE 

FORMATION 


GROUP 

SCALE 

100 

metres 

0 



GREAT SCAR 


NORTH CUMBRIA 

PENNINE UPPER COAL 



MEASURES FM 



ESKETT 

LIMESTONE FM 

2 

M 

PENNINE LOWER 

COAL MEASURES 

FORMATION 

M 

M 

M 

120 

VDMB 

LSMB 

BTL 

RGL 

CGLM 

LTLS 

GL 

FFL 

TYL 

FYL 

SCL 

SPL 

TBL 

JWL 

LLLM 

PGL 

WTL 

LM5 

LM6 

LM7 

v v 

v 

v 

v 

v 

MARSETT FORMATION 

COCKERMOUTH 

VOLCANIC 

FORMATION 

SOLWAY 

FIRTH 

1 


RAVENSTONEDALE GREAT SCAR 

GROUP LIMESTONE GROUP 

OLD RED SANDSTONE SUPERGROUP 

3 

2 

EAST CUMBRIA 

(Shap) 

STAINMORE FM 

ALSTON FM 

SHAP VILLAGE 

LIMESTONE FM 

SHAP WELLS CONGLOMERATE FM 

LOCALITIES 

GREAT LIMESTONE MEMBER 

IPL 

FOUR FATHOM 


THREE YARD LIMESTONE MEMBER 

FIVE YARD LIMESTONE MEMBER 

SCAR LIMESTONE MEMBER 

SPL 

LSRL 

JEW LIMESTONE MEMBER 

LLLM 

ASKL 

TYNE LIMESTONE FM WINTERTARN SANDSTONE 

MEMBER 

KNIPE SCAR 

LIMESTONE FM 

ASHFELL LIMESTONE 

FORMATION 

ASHFELL SANDSTONE 

FORMATION 

MARSETT 

FORMATION 

Figure 14 Cumbria. Representative sections for Carboniferous strata in west, North and east Cumbria. 

Based on George et al. (1976), mitchell (1978), Ramsbottom (1978), and Ramsbottom et al. (1978). The 

profiled location of the numbered sections is given in the inset map. see Appendices 1 and 2 for the names of 

the lithostratigraphical units shown by BGs lexicon of Named Rock units computer codes. m marine band, 

Blue colour indicates named limestone beds; green colour indicates significant developments of named 

sandstone units. dashed lines indicate conjecture; wavy lines indicate unconformity surfaces. 

N 

3 

98001789

wintertarn sandstone member, Tyne limestone Formation 



of the overlying shelly marine mudstone within the Alston 

Formation yoredale facies depositional cycle. 

Thickness 

Between 12 and 14.7 m. 


North Cumbria and edenside, west of pennine–dent Fault 

zone. 

Age 

Asbian to Brigantian. 

6.7.2.2 Jew liMesTone MeMBer (Jwl) 

Name 

No longer bed status, now a member of the Alston Formation. 

see Johnson and dunham (1963); dunham (1990); Burgess 

and Holliday (1979); Trotter and Hollingworth (1932); 

eastwood et al. (1968); Johnson and Nudds (1996). 

Lithology 

limestone, bioclastic, dark grey, thick wavy beds with 

fissile mudstone partings, and usually with abundant 

fossils. At many localities it contains a Saccaminopsis 

band about two-thirds of the thickness above the base 

(Burgess and Holliday, 1979). in Cumbria, the member 

is composed of pale porcellaneous limestone with dark 

irregular spots (pseudobreccias) at the base, overlain by 

well-bedded grey and grey-blue limestone crowded with 

Saccamminopsis fusulinaformis, and in some beds with 

abundant ‘Lithostrotion’ (eastwood et al., 1968). 

Stratotype 

The type section is Force Burn, about 1.2 km upstream 

from its confluence with the River Tees just above the Cow 

Green Reservoir, Teesdale, Cumbria [Ny 771 306] where 

the limestone is fossiliferous and contains many colonial 

corals (Johnson and dunham, 1963, p. 46). A reference 

section is a roadside quarry 730 m e25˚N of the church 

in uldale, Cumbria [Ny 2576 3734], with about 6.5 m 

of dark grey, mostly well-bedded, fossiliferous limestone 

(including a ‘Lithostrotion band’) beneath about 2 m of 

grey-white fossiliferous limestone with red spots (see 

eastwood et al., 1968, p. 171). 


The lower boundary is taken at the sharp base of limestone 

beds overlying a generally conformable ganister sandstone 

of the Alston Formation (Figure 11, Column 1; Figure 14, 

Column 3; Figure 15, Column 1), or north of the lake 

district resting on a few metres of siltstone, mudstone and 

sandstone (Figure 14, Column 2). 

The upper boundary of the member is overlain, generally 

conformably, by siltstone and mudstone of the Alston 

Formation. 

Thickness 

Between 5 and 9.5 m on the Alston Block and 9.1–12.2 m 

north of the lake district massif. 


A member within the Alston Formation of the Alston and 

lake district blocks, and questionably the equivalent of the 

oxford limestone in north Northumberland. it is exposed 

along the North pennine escarpment, on the northern flanks 

121 

of the lake district massif and in the vale of eden, and 

in Teesdale, Cumbria; also in weardale, durham, in the 

Cowgreen–maizebeck area and was formerly seen on 

the site of the Burnhope reservoir in weardale. proved 

at depth in many boreholes and shafts in the northern 

pennines of Northumberland and to the east in durham, 

including the Rookhope Borehole (BGs Registration 

Number Ny94sw/1) [Ny 9375 4278] (Johnson and Nudds, 

1996), the Roddymoor and emma pit (BGs Registration 

Number NZ13Ne/146) [NZ 1513 3435] (woolacott 1923) 

and the seal sands Borehole (BGs Registration Number 

NZ52sw/308) [NZ 538 239]. The Jew limestone is 

apparently absent in the Allenhead’s No 1 Borehole (BGs 

Registration Number Ny84Ne/4) [Ny 8604 4539]. 

Age 

Brigantian. 

6.7.2.3 oxForD liMesTone MeMBer (oxl) 

Name 

Known alternatively as the Greenses limestone. see Frost 

and Holliday (1980); Burgess and Holliday (1979); day 

(1970); Fowler (1926); George and Black (1971); Gunn 

(1900); Gunn and Clough (1895). 

Lithology 

limestone, thick bedded at base, becoming thin bedded at 

top; grey to dark grey with numerous red-weathered Osagia 

(an alga) haloes; particularly rich in corals and brachiopods. 

Stratotype 

The type section is near Broomlee lough, Northumberland 

[Ny 7903 6990 and 7960 7041]. Frost and Holliday (1980, 

p. 32) noted this locality in the grey to dark grey fossiliferous 

limestone with Osagia (‘Girvanella’) haloes, which is 5–6 m 

thick in the Bellingham district (Figure 11, Column 3). 


The lower boundary is taken at the generally conformable, 

sharp base of the first bed of limestone that overlies 

measures of the Alston Formation. This typically displays a 

coal or seatearth immediately below the limestone. 

The upper boundary of the member is taken at the top of 

the uppermost limestone bed that is overlain by a coarsening 

upwards sequence of dark grey mudstones, siltstone and 

sandstone, the first containing ironstone nodules. 

Thickness 



widespread limestone member occurring throughout the 

Northumberland Trough in northern england and the scottish 

Borders within the Alston Formation, stratigraphically lying 

below the eelwell limestone (Figure 12, Column 1–4; 

Figure 13, Column 3). some authors correlate the oxford 

limestone with the Jew limestone of the Alston Block and 

north of the lake district (George and Black, 1971) and with 

the Bridge limestone in the Bewcastle and langholm area 

(day, 1970) (Figure 10, Column 3; Figure 11, Column 2). 

Age 

Brigantian. 

6.7.2.4 TyneBoTToM liMesTone MeMBer (TBl) 

Name 

The member is so-called because it crops out in, or is 

closely underlying, the bed of the River south Tyne 



1 

ROOKHOPE 

BOREHOLE 

NORTHERN ENGLAND DEVONIAN PLUTONIC SUITE 

RVS 


WEARDALE PLUTON MEL 


PENDLETON 

FM 

GREAT 

LIMESTONE 

MEMBER 

FOUR 

FATHOM 

LIMESTONE 

MEMBER 

THREE YARD 

LIMESTONE 

MEMBER 

FIVE YARD 

LIMESTONE 

MEMBER 

SCAR 

LIMESTONE 

MEMBER 

SPL 

TYNE 

BOTTOM 

LIMESTONE 

MEMBER 

JEW 

LIMESTONE 

MEMBER 

LLLM 

SML 

GREAT SCAR 

LIMESTONE 

GROUP 

MARSETT 

FM 



2 

UPPER 

SWALEDALE 



ALSTON FORMATION STAINMORE FM SILSDEN FORMATION 

SCALE 

metres 

M 

M 

50 

0 

‘Water Crag 

Marine Band’ 

3 

GREAT SHUNNER FELL- 

UPPER WENSLEYDALE AND 

LGLL 

RAYDALE BOREHOLE 

E2A1=MKFI 

MKFG 

USTL 

LSTL 

CROL 

PENDLETON 

FORMATION 

LTLS 

STAINMORE 

GL FORMATION 

FFL 

TYL 

FYL 

‘Shunner 

Fell Marine 

Beds’ 

CROL? 

STAINMORE 

FORMATION 

LTLS 

GL 

FFL 

TYL 

FYL 

MDL 

MDL SIL 

SIL 

HSCL 

TYNE 

LIMESTONE 

FORMATION 

GYL 

DANNY BRIDGE 

LIMESTONE 

FORMATION 

GARSDALE 

LIMESTONE 

FORMATION 

FAWES WOOD 

LIMESTONE 

FORMATION 

TOM CROFT 

LIMESTONE 

FORMATION 

PENNY FARM 

GILL FORMATION 


SILSDEN FORMATION 




RAVENSTONEDALE GROUP 

MARSETT FM 

WHERNSIDE- 

KINGSDALE- 

INGLEBOROUGH 

MILLSTONE 

GRIT GROUP 

LGLL 

HSCL 

GYL 

Gap in 

HWL 

WINTERTARN 

SANDSTONE 

MEMBER 

RAYDALE DOLOSTONE 

FORMATION 

PENDLETON 

FORMATION 

ASHFELL 

SANDSTONE 

FORMATION 

GREAT SCAR LIMESTONE GROUP YOREDALE GROUP 

MALHAM FORMATION 

ALSTON FORMATION SILSDEN FM 

PENNINE COAL 

MEASURES 

GROUP 

ROSSENDALE FORMATION 

MARSDEN 

FORMATION 

122 

4 

HEBDEN FORMATION 

KILNSEY 

FORMATION 

SAMLESBURY 

FORMATION 

PENDLETON 

FORMATION 

GL 

FFL 

TYL 

MDL 

SIL 

HSCL 

GYL 

HWL 

N 

Morecambe 

Bay 

5 

COLSTERDALE- 

NIDDERDALE- 

GREENHOW 


SILSDEN FORMATION 




GARSDALE LIMESTONE FORMATION DANNY BRIDGE LIMESTONE FM 

LOCALITIES 

4 

PENNINE LOWER COAL 


M 

M 

M 

3 

6 

G1B1 

G1A1 

H1B1 

ISMB? 

CMB 

2 

MILLSTONE 

GRIT GROUP 

BOWLAND 

SHALE 

FORMATION 

E2A1 (CHMB) 

=’MKFI’ 

‘Upper Toft 

Gate Limestone’ 

=MDL 

‘Lower Toft 

Gate Limestone’ 

=SIL 

M 

‘Coldstones 

GVB Limestone’ 

HGEL 

GNWL 

SCSL 

‘Timpony 

Limestone’ 

CHAPEL 

HOUSE 

LIMESTONE 

FORMATION 

1 

MALHAM COVE- 

GORDALE SCAR 

‘TRANSITION ZONE’ 

5 

GREAT SCAR LIMESTONE GROUP YOREDALE GP CRAVEN GP 

KILNSEY FORMATION 

MALHAM FORMATION 

ALSTON FM 

98001790 

6 

PENDLETON FORMATION 

PENDLE 

GRIT 

MEMBER 

SIL 

HSCL 

GYL 

HWL 

STOCKDALE FARM 

FORMATION 

GORDALE 

LIMESTONE 

MEMBER 

COVE 

LIMESTONE 

MEMBER 

SCALEBER 

QUARRY 

LIMESTONE 

MEMBER 

SCALEBER 

FORCE 

LIMESTONE 

MEMBER

Figure 15 (opposite) Askrigg Block. Representative 

sections for Carboniferous strata various localities including at 

upper swaledale, Great shunner Fell–upper wensleydale and 

the Raydale Borehole, whernside–Kingsdale–ingleborough, 

Colsterdale–Nidderdale–Greenhow, and the malham Cove– 

Gordale scar ‘Transition Zone’, together with a summary log 

of the Rookhope Borehole, Alston Block to provide 

correlation of members and individual limestones within the 

Alston Formation between the Askrigg and Alston blocks. 

Based on dunham et al. (1965), dunham and wilson (1985) 

and Arthurton et al. (1988). see Appendices 1 and 2 for the 

names of the lithostratigraphical units shown by BGs lexicon 

of Named Rock units computer codes. m marine band; Blue 

colour indicates named limestone beds: green colour indicates 

significant developments of named sandstone units. dashed 

lines indicate conjecture; wavy lines indicate unconformity 

surfaces. 

between Alston and Tynehead. it no longer has bed status 

(i.e. the Tyne Bottom limestone of, for example, Trotter 

and Hollingworth, 1932), but is now a member of the 

Alston Formation. see Johnson and dunham (1963); 

dunham (1990); Burgess and Holliday (1979); eastwood 

et al. (1968); Johnson and Nudds (1996); Arthurton and 

wadge (1981). 

Lithology 

limestone, blue-grey, thick-bedded, planar to wavybedded, 

stylolitic, in part fissile with intercalated thin 

mudstone beds. Fossiliferous, particularly with abundant 

corals, brachiopods and crinoid debris. it commonly has 

a Saccamminopsis band 1.5 to 2 m from the top. A bed 

near the top is characteristically argillaceous and ‘slaggy’ 

(Johnson and dunham 1963). 

Stratotype 

The type area is High Cup Gill, dufton Fell, Cumbria 

[Ny 730 250 to 752 274] where about 8 m of limestone 

are exposed (see Burgess and Holliday, 1979, fig. 26, 

col. 6). A reference section is the Rookhope Borehole 

(BGs Registration Number Ny94sw/1) [Ny 9375 4278] 

from 175.62 to 184.94 m depth (Johnson and Nudds, 

1996). 



overlying measures within the Alston Formation, in places 

comprising sandstone, elsewhere mudstone. 


of overlying measures within the Alston Formation, here 

usually comprising up to about 10 m of compact, hard, dark 

grey mudstone colloquially referred to as the Tyne Bottom 

plate. 

Thickness 

Between 7.6 and 14.6 m. 


The member crops out in, or closely underlies, the bed of 

the River south Tyne between Alston and Tynehead. The 

limestone is well exposed along the pennine escarpment in 

Teesdale and weardale. it is well known from subsurface 

workings, boreholes and shafts within the Alston Block. The 

member occurs within the Alston Formation of the Alston 

and lake district blocks in Cumbria, Northumberland 

and durham, lying between the Jew (below) and the 

123 

scar (above) limestone members (Figure 11, Column 1; 

Figure 14, Column 2). it is present in the Rookhope 

Borehole (Figure 15, Column 1) (see above) and the 

Allenheads No. 1 Borehole (BGs Registration Number 

Ny84Ne/4) [Ny 8604 4539]. 


Brigantian. Cozar and somerville (2004) record a single 

specimen of the foraminifer Asteroarchaediscus from the 

Tynebottom limestone member in the Rookhope Borehole 

(see above). This genus is only present in the uppermost 

lower Brigantian and mostly occurs in the upper Brigantian 

(Cozar and somerville, 2004 and references therein). 

6.7.2.5 eelwell liMesTone MeMBer (ewl) 

Name 

previously known as the Harelawhill limestone. see Frost 

and Holliday (1980); Chadwick et al. (1995); day (1970); 

Gunn (1900); lumsden and wilson (1961). 

Lithology 

limestone, grey, bioclastic, generally devoid of mudstone 

partings; typically rich in algal remains with a prominent 

fauna of brachiopods and corals; appreciably dolomitised 

in part, giving a brown-weathered and vuggy appearance. 

Stratotype 

The type areas are near walwick, about 2 km west of 

Chollerford, Northumberland [Ny 8878 7033 to 9083 

7116] where Frost and Holliday (1980, p. 36) referred to 

the typically massive, grey, bioclastic limestone, devoid 

of mudstone partings, being well exposed; and Cargie’s 

plantation [Nu 024 495] to saltpan Rocks [Nu 025 490], 

seahouses, approximately 3 km south-east of Berwickupon-Tweed, 

Northumberland where Fowler (1926, p. 25) 

described the limestone exposed on the shore as browned (as 

if dolomitised), steeply dipping, contorted and fossiliferous. 




measures of the Alston Formation; typically sandstone. 


the uppermost limestone bed that is overlain by a sequence 

of dark grey mudstones and siltstones, containing ironstone 

nodules locally. 

Thickness 



A widespread limestone member within the Alston 

Formation, occurring throughout the Northumberland 

Trough in northern england and the scottish Borders, 

stratigraphically lying below the Three yard limestone 

and above the oxford limestone (Figure 11, Column 3; 

Figure 12, Columns 1–4). This definition incorporates its 

correlated unit in the langholm and Bewcastle areas of the 

scottish Borders region, the Harelawhill limestone. 

Age 

Brigantian. 

6.7.2.6 sCar liMesTone MeMBer (sCl) 

Name 

Named after the limestone exposures along the pennine 

escarpment. see Arthurton and wadge (1981); dunham 

(1990); Burgess and Holliday (1979); Trotter and Hollingworth 



(1932); eastwood et al. (1968); Johnson and Nudds (1996); 

Johnson et al. (1980); Johnson and dunham (1963). 

Lithology 

limestone, pale to mid grey, wavy-bedded, crinoidal with 

fissile uppermost part and shaly partings; stylolitic. it 

is generally fossiliferous with bands of Siphonodendron 

junceum. Comparatively unfossiliferous in the south, 

though a bed rich in brachiopods is present at the base 

in the southern part of the Brough district (Burgess and 

Holliday 1979). Nodules of chert are commonly found in 

this limestone (Trotter and Hollingworth, 1932; dunham, 

1990). in the longcleugh No. 1 Borehole (Johnson et 

al., 1980), Allenheads No. 1 Borehole (BGs Registration 

Number Ny84Ne/4) [Ny 8604 4539] and Rookhope 

Borehole (BGs Registration Number Ny94sw/1) [Ny 

9375 4278] the upper part of the member includes an 

interbedded unit of black pyritic fossiliferous mudstone 

with sporadic small ironstone nodules. 

Stratotype 

The type section is in a disused quarry north-east of 

Croglin, Cumbria [Ny 5834 4815 to 752 274] the scar 

limestone is 14.6 m thick with the lower 9.8 m of massive 

grey limestone, separated from rather darker beds with thin 

mudstone partings above, by 0.6 m of calcareous mudstone 

(see Arthurton and wadge, 1981, p. 42). A reference section 

is the Rookhope Borehole (see above), in which the scar 

limestone, including a 1.62 m thick mudstone interbed, 

occurs from 137.95 to 147.26 m depth (see Johnson and 

Nudds, 1996, p. 191). 



overlying measures within the Alston Formation; directly 

underlain locally by dark mudstone, seatearth sandstone or 

by a coal seam. 


of overlying strata within the Alston Formation typically 

comprising cyclical sedimentary rocks with thickly bedded, 

commonly bioclastic, limestones 

Thickness 



The member falls within the Alston Formation of the Alston 

and lake district blocks in Cumbria, Northumberland and 

durham, and lies stratigraphically between the Tynebottom 

(below) and the Five yard (above) limestone members 

(Figure 11, Column 1; Figure 14, Column 2; Figure 15, 

Column 1). The limestone is well exposed along the 

pennine escarpment, in Teesdale and weardale. it is well 

known from subsurface workings, boreholes and shafts 

within the Alston Block. it is present in deep boreholes 

including longcleugh No 1 Borehole in the west Allen 

valley (Johnson et al., 1980), and the Rookhope and the 

Allenheads No. 1 boreholes (see above). 

Age 

Brigantian. Goniatites of the Lusitanoceras granosus p2a subzone are found in mudstone just above the limestone at 

Bowlees in Teesdale. 

6.7.2.7 Five yarD liMesTone MeMBer (Fyl) 

Name 


see Arthurton and wadge (1981); dunham (1990); Burgess 



124 

and Holliday (1979); Trotter and Hollingworth (1932); 

eastwood et al. (1968); Johnson and Nudds (1996); Johnson 

et al. (1980). 

Lithology 

limestone, dark grey, argillaceous, becoming grey compact 

towards base. in the south, fine-grained with thin evenly 

bedded mudstone partings with many fossils; in the north 

becoming increasingly crinoidal and locally characterised 

by coarse crinoidal debris. intercalated thin unit (up to 2.1 

m thick) of black fossiliferous calcareous mudstone which 

divides the member into two parts. stylolitic particularly 

near the base (Johnson and Nudds, 1996). 

Stratotype 

The type section is at lunchy Beck [Ny 6036 4822], a 

northern tributary of Croglin water, Cumbria, where the 

Five yard limestone is a dark blue-grey, thick-bedded 

limestone with muddy partings, 4.9 m thick (Arthurton and 

wadge, 1981, pp. 43–44). A reference section is provided 

by the Rookhope Borehole (BGs Registration Number 

Ny94sw/1) [Ny 9375 4278] from 109.7 to 114.3 m depth 

including a 0.53 m-thick interbed of black fossiliferous 

calcareous shale (see Johnson and Nudds, 1996, p. 190). 


The lower boundary is taken at the sharp base of the limestone 

overlying measures within the Alston Formation. it is 

directly underlain by burrowed, current and ripple-bedded, 

medium-grained sandstone; a thin coal is present in places. 


of the overlying mudstone within measures of the Alston 

Formation. 

Thickness 


Distribution and regional correlation: 

A member within the Alston Formation of the Alston and 

lake district blocks in Cumbria, Northumberland and 

durham, lying stratigraphically between the scar (below) 

and the Three yard (above) limestone members (Figure 11, 

Column 1; Figure 14, Columns 2, 3; Figure 15, Column 1). 

possibly correlated with the eelwell limestone member of 

the Northumberland Trough. The limestone is well exposed 

along the pennine escarpment in Teesdale and weardale. 

it is well known from subsurface workings, boreholes 

and shafts within the Alston Block. it is present in deep 

boreholes including the longcleugh No 1 Borehole in the 

west Allen valley (Johnson et al., 1980), and the Rookhope 

and Allenheads No. 1 boreholes (see above). 

Age 

Brigantian. on dun Fell the limestone has yielded goniatites 

indicating the Neoglyphioceras subcirculare p2b subzone 

(Johnson and dunham, 1963; dunham, 1990). in the 

Rookhope Borehole (see above) the first appearance of the 

foraminifers Janischewskina typica and Endothyranopsis 

sphaerica, and the alga Calcifolium okense indicate the late 

Brigantian upper Cf6 subzone (see Cozar and somerville, 

2004). 

6.7.2.8 THree yarD liMesTone MeMBer (Tyl) 

Name 

Formerly the Acre limestone of Northumberland, and the 

Third limestone of north of the lake district. The Three 

yard limestone bed now has member status. see mills and 

Hull (1976); Burgess and Holliday (1979); Chadwick et al.

(1995); day (1970); dunham (1990); dunham and wilson 

(1985); eastwood et al. (1968); Frost and Holliday (1980); 

Gunn (1900); Johnson et al. (1962); Johnson and Nudds 

(1996); lumsden and wilson (1961); young and Boland 

(1992). 

Lithology 

limestone, packstone, fine-grained, mid and dark grey, 

thickly bedded; fissile and nodular in part, with styolites; thin 

mudstone partings, particularly in north Northumberland. 

Crinoid debris and foraminifers are typically characteristic, 

but the member is not particularly fossiliferous on the Alston 

Block. on the Askrigg Block, the limestone is split into two 

leaves by a ganister-like sandstone which thickens to up to 

8 m westwards (Burgess and Holliday, 1979; dunham and 

wilson, 1985); a thin coal is shown at a similar horizon in 

the Barnard Castle district to the east (mills and Hull, 1976). 

Stratotype 

The type area is coastal exposures at saltpan Rocks [Nu 

026 493 to 026 481], about 3 km south-east of Berwickupon-Tweed, 

Northumberland where Fowler (1926, p. 25) 

described the limestone exposed on the shore below tidemark 

as pale grey, dipping eastward at about 12˚, folded, 

and with marine fossils (including Saccamminopsis) about 

4.5 m thick. The type section is in the River Greta at 

scotchman’s stone [Ny 0807 1245], about 8 km east of 

Bowes, Co. durham where the limestone is 3.66 m thick 

and includes shale partings and a 3.5 cm coal (see mills and 

Hull, 1976, p. 15). 




measures of the Alston Formation. on the Alston Block, 

it usually lies above a major sandstone body referred to as 

the six Fathom Hazle. This typically displays a seatearth 

below the limestone, and in north Northumberland there is 

typically a coal; also, a few tens of centimetres of mudstone 

may intervene locally. 

The upper boundary of the member is taken at the 

top of the uppermost limestone bed that is overlain by a 

sequence of dark grey mudstones and siltstones, in north 

Northumberland containing ironstone nodules locally. 

Thickness 

Between 1.8 and 4.6 m on the Alston Block; 3–10 m in the 

whitehaven to Gilcrux district, north of the lake district; 

an average of 2.7 m on the Askrigg Block; 5–6 m in 



widespread limestone member occurring throughout 

northern england and the scottish Borders within the 

Alston Formation, stratigraphically lying below the Four 

Fathom limestone and above the Five yard limestone 

on the Alston Block (Figure 11, Column 1; Figure 14, 

Columns 2, 3; Figure 15, Columns 1–3) or the eelwell 

limestone in Northumberland (Figure 11, Column 3; 

Figure 12, Columns 1–4; Figure 13, Column 4). This 

definition incorporates its other local names of Acre 

limestone in Northumberland and Third limestone of 

Cumbria (eastwood et al., 1968; young and Boland, 

1992). Geographical distribution therefore includes 

Cumbria, Northumberland, durham and North yorkshire. 

The member has been seen in numerous deep boreholes 

throughout the region including the Archerbeck Borehole 

(BGs Registration Number Ny47Nw/14) [Ny 4160 

125 

7820] (lumsden and wilson, 1961), the Rookhope 


9375 4278] (Johnson and Nudds, 1996), the Barrock park 


4613 4660], the Throckley Borehole (BGs Registration 

Number NZ16Nw/45) [Ny 1456 6762], the Harton 

Borehole (BGs Registration Number NZ36Ne/80) [NZ 

3966 6563], the woodland Borehole (BGs Registration 

Number NZ02Ne/4) [NZ 0910 2769] and the seal sands 

Borehole (BGs Registration Number NZ52sw/308) [NZ 

538 239]. The member has also been widely seen on the 

Alston Block in many mine shafts and workings. 

Age 

Brigantian. A goniatite indicative of the Lyrogoniatites 

georgiensis p2c subzone has been recorded from 

mudstones above the Three yard limestone (Johnson et 

al., 1962). 

6.7.2.9 Four FaTHoM liMesTone MeMBer (FFl) 

Name 


previously known as the Four Fathom limestone, sandbanks 

limestone, low dean limestone (Gunn, 1900), eight 

yard limestone, second limestone, Buccleuch limestone 

(lumsden and wilson, 1961), undersett limestone. see 

also Burgess and Holliday (1979); Chadwick et al. (1995); 

day (1970); dunham (1990); dunham and wilson (1985); 

eastwood et al. (1968); Frost and Holliday (1980); Holliday 

et al. (1975); Johnson et al. (1962); Johnson and Nudds 

(1996); young and Boland (1992). 

Lithology 

limestone, packstone, fine-grained, mid and dark grey, 

thick bedded and wavy-bedded, with few mudstone 

partings; somewhat argillaceous, particularly at the top. 

Typically contains layers of nodules and lenses of black 

chert. Crinoidal but not particularly fossiliferous on the 

Alston Block; contains conspicuous coral biostromes to the 

north and south of the Alston Block. 

Stratotype 

The type area is coastal exposures of Near skerr, middle 

skerr and Far skerr, about 4 km south-east of Berwickupon-Tweed 

[Nu 028 487 to 036 481]. Here the limestone 

is earthy and bluish with many shale partings, about 

8.5 m thick (Fowler, 1926, pp. 26–27). The type section 

is the middlehope Burn, westgate, upper weardale 

[Ny 905 396] where a nearly complete section can 

be seen. A reference section is the Rookhope Borehole 

(BGs Registration Number Ny94sw/1) [Ny 9375 4278] 

Rookhope, weardale, Co. durham from 57.99 to 63.70 m 

depth (see Johnson and Nudds, 1996, p. 187). 



sharp base of the first bed of limestone that overlies strata 

of the Alston Formation. on the Alston Block, it usually 

overlies less than 2 m of dark grey seatearth mudstone and 

mudstone with abundant plants that overlies a prominent 

sandstone referred to there as the Natrass Gill Hazle. in the 

Bellingham district a coal underlies the limestone. 



of dark grey mudstones, the lowermost of which are calcareous 

and fossiliferous. on the Askrigg Block the limestone 

member is overlain by a dark grey or almost black chert 

called the underset Chert. 



Thickness 

Between 7 and 10 m north of the lake district and in 

Northumberland; 5–12 m on the Alston Block; about 9 m 

on the Askrigg Block, but locally up to 25 m. 


occurs throughout northern england and the scottish 

Borders, lying below the Great limestone near the top of 

the Alston Formation (Figure 10, Column 3; Figure 11, 

Columns 1–3; Figure 12, Columns 1, 3, 4; Figure 13, 

Columns 3, 4; Figure 14, Columns 2, 3; Figure 15, 

Columns 1–4). This definition incorporates the various 

other local names of sandbanks, lowdean and eight yard 

in Northumberland, the Buccleuch limestone (lumsden 

and wilson, 1961) of the langholm and Bewcastle area; 

the second limestone of Cumbria (eastwood et al., 1968; 

young and Boland, 1992) and the underset limestone 

of the Askrigg Block (for example dunham and wilson, 

1985). Geographical distribution therefore includes 

Cumbria, Northumberland, durham and North yorkshire. 


throughout the region including the Archerbeck Borehole 

(BGs Registration Number Ny47Nw/14) [Ny 4160 7820] 

(lumsden and wilson, 1961), the Rookhope Borehole 

(see above), the Barrock park Borehole (BGs Registration 

Number Ny44Ne/28) [Ny 4613 4660], the Throckley 

Borehole (BGs Registration Number NZ16Nw/45 [NZ 

1456 6762], the Harton Borehole (BGs Registration 

Number NZ36Ne/80) [NZ 3966 6563], the woodland 


0910 2769] and the seal sands Borehole (BGs Registration 

Number NZ52sw/308) [NZ 538 239]. The member has 

also been widely seen on the Alston Block in many mine 

shafts and workings. 

Age 

Brigantian. Goniatites indicative of the Lyrogoniatites 

georgiensis p2c subzone have been found in mudstones 

above the Four Fathom limestone in the mount pleasant 

Borehole [NZ 034 152] near Barnard Castle (Johnson et 

al., 1962). 

6.7.2.10 greaT liMesTone MeMBer (gl) 

Name 

No longer bed status, now a member of the Alston 

Formation (yoredale Group). The member includes the 

former main limestone of the Askrigg Block, the Catsbit 

limestone of langholm, and the dryburn limestone of 

Northumberland. see Cossey et al. (2004), and Burgess 

and Holliday (1979); Chadwick et al. (1995); day (1970); 

dunham (1990); dunham and wilson (1985); eastwood et 

al. (1968); Fairbairn (1978, 1980, 2001); Johnson (1958); 

Johnson and Nudds (1996); lumsden and wilson (1961); 

young and Boland (1992). 

Lithology 

limestone (bioclastic packstone), mid to dark blue-grey; 

thickly bedded with thin shaly mudstone partings along 

uneven or wavy bedding planes; there is much crinoid 

debris throughout and there are many other beds rich in 

brachiopods and/or corals. The internal stratigraphy of 

the member is in parts remarkably consistent throughout 

the region and four informal divisions are recognised 

(Fairbairn, 1980) and referred to, from the base upwards 

as the Bench, main and Transitional posts and the Tumbler 

Beds. Beds rich in fossils are widespread. most notable 

and widespread is the Chaetetes Band (Johnson, 1958) 

which occurs near the base; this comprises a sponge 



126 

biostrome along with locally abundant brachiopods, corals 

and ostracods. within the main posts are the Brunton 

Band comprising the rare alga Calcifolium (Johnson, 1958; 

Cossey et al., 2004), and the Frosterly marble (Johnson, 

1958). At the top, the Tumbler Beds, typically 2–5 m 

thick, comprise thick beds of limestone interbedded with 

persistent mudstone units. 

Stratotype 

The type section is Greenleighton Quarry, about 10 km south 

of Rothbury, Northumberland [NZ 034 917] (Figure 13, 

Column 3), which includes 12 m of limestone divisible into 

the Bench, main and Transitional posts and Tumbler Beds 

of Fairbairn (1980) (see Cossey et al., 2004, pp. 144–147). 

Reference sections occur at Brunton Bank Quarry, about 

1 km south-east of Chollerford, Northumberland [Ny 

928 699] where the Great limestone is about 15 m thick 

and contains the type sections of the Brunton Band (with 

the rare alga Calcifolium), and the Chaetetes Band (a 

spectacular sponge biostrome) (see Cossey et al., 2004, pp. 

141–144); eastgate Quarry, weardale, Co. durham [Ny 

940 370] where a complete section, including the Frosterly 

marble, can be seen; Tendley Hill Quarry, Cumbria [Ny 

088 289] where a full thickness of 15.8 m of mid grey, 

thickly bedded, prominently jointed packstone, typically 

with uneven or wavy bedding planes, and a development 

of the Chaetetes Band can be seen (young and Boland, 

1992, p. 21); the Archerbeck Borehole (BGs Registration 

Number Ny47Nw/1) [Ny 4157 7815], 2 km north-east of 

Canonbie, dumfriesshire from 215.8 to 238.3 m depth with 

massive limestone except for a few calcareous mudstone 

beds (see lumsden and wilson, 1961); and the Rookhope 


9375 4278], Rookhope, weardale, Co. durham from 

rockhead, apparently near the top of the limestone at 6.86 

to 25.07 m depth (see Johnson and Nudds, 1996, p. 185). 



sharp base of the first bed of limestone that overlies strata 

of the Alston Formation (which is characterised by cyclical 

sedimentary rocks that include thick-bedded, commonly 

bioclastic limestones). in most localities the limestone 

directly overlies the Tuft sandstone, a brown, micaceous 

fine-grained sandstone that has a rooty upper part and which 

locally may be overlain by a thin carbonaceous smear or a 

coal. 



of dark grey siltstones and mudstones at the base of the 

stainmore Formation (smGp). 

Thickness 

About 12 m in the vale of eden; 16–22 m on the Alston 

Block; 22–24 m with a maximum of 40 m on the Askrigg 

Block and 8–15 m in the Northumberland Trough; about 

22 m in the langholm area and Archerbeck Borehole. 


occurs throughout most of northern england at the top 

of the Alston Formation. This definition incorporates the 

main limestone of the Askrigg Block, and the Catsbit 

limestone (day, 1970) of the scottish Borders near 

langholm. Geographical distribution therefore includes, 

Northumberland, durham and North yorkshire. The Great 

limestone has also been correlated with the the First 

limestone (lm1) (eskett limestone Formation, Great 

scar limestone Group) of Cumbria (Figure 14, Column 1),

and the Top Hosie limestone (ToHo) (lower limestone 

Formation, Clackmannan Group) of the midland valley of 

scotland (Figure 6, Column 4). 


throughout the region including the Archerbeck 

and Rookhope boreholes (see above), the Barrock park 


4613 4660], the Throckley Borehole (BGs Registration 

Number NZ16Nw/45 [NZ 1456 6762], the Harton 


3966 6563], the woodland Borehole (BGs Registration 

Number NZ02Ne/4) [NZ 0910 2769] and the seal sands 

Borehole (BGs Registration Number NZ52sw/308) [NZ 

538 239] (Chadwick et al., 1995). 

Age 

pendleian. At Fountains Fell on the Askrigg Block the 

Great limestone (formerly the main limestone) overlies 

mudstone with the e 1a subzone ammonoid Cravenoceras 

(=Emstites) leion (Arthurton et al., 1988). A change in 

foraminiferal assemblage at the base of the Catsbit limestone 

(the local equivalent of the Great limestone member) in the 

Archerbeck Borehole (see above) suggests that the base of 

the Namurian occurs at this level (Cummings, 1961). 

6.7.3 Stainmore Formation (SMGP) 

Name 

The name is derived from the former stainmore Group, 

a chronostratigraphical term for the entire Namurian 

succession (Burgess and Holliday, 1979). in west Cumbria 

the stainmore Formation now replaces the Hensingham 

Group of Akhurst et al. (1997). 

Lithology 

The stainmore Formation comprises a cyclical succession 

of sedimentary rocks, with repetitive mudstones, laminated 

siltstones, sandstones, thin limestones and thin coals. it is 

distinguishable from the underlying Alston Formation by 

a decrease in the number and thickness of the limestones, 

which also tend to be darker grey and more impure. 

it extends from the top of the Great limestone (or a 

correlative) to the base of the subcrenatum marine Band 

(sBmB) (or its equivalent) at the base of the pennine Coal 

measures Group. The limestones, which are more prominent 

in the south of the Askrigg Block, are dark grey with a 

diverse marine fauna. limestones are rare or absent from 

the upper part of the formation. The sandstones are typically 

fine- to medium-grained, white to pale brown, commonly 

bioturbated and rooty. The mudstones may be very dark 

grey. on the Askrigg Block there are up to four main levels 

of chert within the formation, typically developed above 

the limestone component of the cyclothem. The Richmond 

Chert is the thickest at up to 40 m thick. it contains sponge 

spicules and displays rapid lateral transitions to crinoidal 

limestones. in west Cumbria the succession includes 

distinct, laterally discontinuous, major channel sand bodies, 

such as the Hensingham Grit and has an unusual limestone 

development the ‘Tylonautilus’ or snebro Gill Beds. At 

Canonbie, the stainmore Formation is poorly exposed, 

but comprises repetitive cycles of sandstone, siltstone and 

claystone with thin beds of coal. 

[it should be noted that the formerly widespread use 

across Northumberland and durham, of the term ‘millstone 

Grit’ to encompass sandstone-rich beds beneath undoubted 

Coal measures rocks, appears to be traceable back to the 

long-obsolete threefold division of the British Carboniferous 

sequence into mountain limestone, millstone Grit and Coal 

127 

measures. whereas the first and third of these divisions could 

be readily recognised, it is clear that the original geological 

surveyors felt constrained, apparently with some difficulty, 

to define representatives of the millstone Grit, even as 

recently as the latter half of the 20th century. Accordingly, 

beds between the former upper limestone Group and Coal 

measures in Northumberland, and between the former Alston 

Group and Coal measures of the Northern pennines, have 

been classified as millstone Grit. This usage was applied 

as recently as 1989 in the compilation of Geological sheet 

20 (Newcastle upon Tyne), though further confusion was 

introduced here with the synonymous use of the term 

stainmore Group to classify these rocks. A more cautious, 

and arguably realistic, approach had previously been adopted 

on Geological sheet 13 (Bellingham). Here the succession 

above the liddesdale Group was classified as stainmore 

Group, with no reference to millstone Grit. dunham (1990, 

p. 36) drew attention to the difficulty of correlating sandstones 

beneath the Coal measures with the classic millstone 

Grit of the mid pennines, yorkshire and lancashire, adding 

that the difficulty of making this correlation had by then been 

appreciated for at least half a century. 

whereas use of the term millstone Grit cannot at present 

be justified in this part of northern england, it is 

important to recognise that coarse-grained sandstone bodies, 

which exhibit many ‘millstone Grit’ characteristics 

with strongly erosive bases and with channel-like morphologies 

are present within the succession classified as 

the stainmore Formation. Current knowledge indicates that 

these are present at several horizons within the stainmore 

Formation succession, though no clear evidence has yet 

emerged to view these as other than local lithofacies variations 

within the rocks classified as stainmore Formation. 

in Northumberland such sand bodies include the Rothley 

and shaftoe Grits of Geological sheets 14 (morpeth) and 9 

(Rothbury), which exhibit deep erosive bases close to the 

horizons of the little and oakwood limestones respectively 

(young and lawrence, 2002). Although not recently 

mapped in detail, the longhoughton Grits of Geological 

sheet 6 (Alnwick) appear to comprise a channel-based 

sandstone at the horizon of the Foxton limestones. in 

all of these cases there is evidence of contemporaneous 

tectonic control on sedimentation. Clearly, in these examples, 

‘millstone Grit’-like sandstones occur at a variety of 

stratigraphical levels, and are underlain and overlain by 

successions of rocks characteristic of the stainmore Group 

lithofacies. 

Notwithstanding dunham’s (1990) comments on the 

stratigraphical affinities of certain coarse-grained, locally 

pebbly sandstones, noted above, evidence from recent mapping 

of the northern margin of the Alston Block (whitfield 

to Hexhamshire Common) has shown that coarse-grained, 

channel, sand-bodies dominate the succession in the upper 

part of the stainmore Formation. Thus, in this area, the formation 

comprises a lower division consisting of mudstone 

interbedded with tabular units of fine and medium-grained 

sandstone and thin limestone beds, and an upper division 

of coarse-grained sandstone, lacking limestone. work in 

progress on the Alston Block will determine the distribution 

and significance of this upper division and hence its 

lithostratigraphical status.] 


Cyclical marine and deltaic environments. 

Stratotype 

The type area of the stainmore Formation is the stainmore 

Trough. Reference sections include mousegill Beck (BGs 



Registration Number Ny81sw/7) [Ny 8369 1242] from the 

base of the subcrenatum (swinstone Top) marine band at 

136.25 m depth to the top of the Great limestone at 582.47 

m depth (see Burgess and Holliday, 1979) and the Throckley 

Borehole (BGs Registration Number NZ16Nw/45) [NZ 

1456 6762] from about 69 to 577 m depth. in west Cumbria 

the formation occurs in the distington Borehole (BGs 

Registration Number NX92se/84) [NX 9972 2334] from 

below the inferred position of the subcrenatum marine 

Band (sBmB) at about 20 m depth to the top of the First 

limestone, eskett limestone Formation, at about 121 m 

depth (see Akhurst et al., 1997, fig. 24); the Rowhall 

Farm Borehole (BGs Registration Number Ny03Ne/49) 

[Ny 0851 3664] from the non-sequence at about 61.5 m 

depth to the top of the First limestone, eskett limestone 

Formation, at about 203.2 m depth (see Akhurst et al. 1997, 

fig. 24; Brand, 2003); Bigrigg Quarry (disused) [Ny 0052 

1270] which includes yeadonian strata (see eastwood et 

al., 1931; Akhurst et al., 1997); Brigham Quarry (disused) 

[Ny 083 302] which exposes more than 30 m thickness of 

the Hensingham Grit which is locally developed at the base 

of the formation (see young and Boland, 1992; Akhurst et 

al., 1997); and snebro Gill [NX 9835 1685] where stream 

sections and cuttings in the Hensingham inlier include 

impure marine limestones and mudstones. 


The base of the formation is conformable on the Great 

limestone member (or correlatives) at the top of the Alston 

Formation (Figure 6, Column 7; Figure 8, Columns 11, 12; 

Figure 9, Columns 13, 5–7; Figure 10, Column 3; Figure 

11, Columns 1, 3; Figure 12, Columns 1, 3, 4; Figure 13, 

Columns 3, 4; Figure 14, Columns 2, 3; Figure 15, Columns 

2–4). However, in west Cumbria, in the egremont– 

whitehaven–maryport–Cockermouth area, the lower 

boundary occurs where the shelf carbonate sequence of the 

First limestone member is terminated and conformably 

overlain by the mostly clastic marine and deltaic facies of 

the stainmore Formation (Figure 14, Column 1). Here, at 

outcrop the basal part of the stainmore Formation generally 

comprises the coarse-grained, fluvial, Hensingham Grit 

with a thin basal mudstone. 

The top of the formation is generally conformable 

beneath the subcrenatum marine Band (sBmB) at the base 

of the mostly fluviodeltaic mudstones, siltstones and sandstones 

of the pennine lower Coal measures (plCm), or at 

the base of the coal-bearing sequence if this marker band (or 

an equivalent) cannot be identified. 

on the Askrigg Block, the top of the formation is at the 

base of the pendleton Formation, millstone Grit Group 

(Figure 9, Column 17; Figure 15, Columns 2–4). Here, 

the mixed shelf carbonate and deltaic succession of the 

stainmore Formation is succeeded, at an unconformity of 

e1c age by sandstone-dominated strata (see Brandon et al., 

1995). 

in the Canonbie Coalfield, the boundary with the pennine 

lower Coal measures Formation is uncertain in both position 

and nature. The subcrenatum marine Band has not 

been recognised here, and the unconformities inferred by 

lumsden et al. (1967) and picken (1988) have been discounted 

by Jones and Holliday (2006) on sedimentological 

and seismic reflection evidence. 

Thickness 

The formation tends to thicken into troughs and half-grabens. 

in north and west Cumbria it thickens northwards, the 

relatively thin succession on the lake district Block being 

separated from the solway Basin by the syndepositional 



128 

maryport Fault (Barnes et al., 1988; Chadwick et al., 

1995). The formation is 50 m thick in the lamplugh area 

(young and Boland, 1992) and 110 m and 140 m thick in 

the distington and Rowhall Farm boreholes respectively 

(Akhurst et al., 1997). over 500 m of strata are present 

in boreholes north of maryport (Ramsbottom, 1978). The 

thickest development on the Askrigg Block is about 180 m 

at the northern margin where the deltaic component of the 

cyclothems is thicker. The formation is up to 200 m thick in 

the Appleby district. Around Canonbie, seismic reflection 

data indicate that the formation is more than 400 m thick. 


Northern england, north of the Askrigg Block, including 

west Cumbria. 


Namurian (pendleian to yeadonian). The type localities of 

the yeadonian ammonoids Cancelloceras cancellatum and 

Gastrioceras cumbriense occur within the mudstone beds 

at Bigrigg [Ny 0010 1305]. in west and north Cumbria 

the formation is also pendleian to yeadonian, but there is 

a large non-sequence above the snebro Gill Beds in which 

strata of Chokierian to marsdenian age are absent (Akhurst 

et al., 1997). The limestones that are more prominent in 

the south of the Askrigg Block notably include crinoid 

debris and the nautiloid Tylonautilus nodiferus. The first 

appearance of common Crassispora kosankei miospores 

about 14 m above the base of the first thick sandstone 

(‘First Grit’) in the Throckley Borehole (see above) marks 

the base of the Kv Zone (stephenson et al., 2008) of 

Kinderscoutian age. The upper 140 m of the stainmore 

Formation in the langholm area includes strata of the FR 

miospore Zone (late marsdennian to yeadonian in age) in 

the Rowanburnfoot Borehole (BGs Registration Number 

Ny47Nw/27) [Ny 41031 75743] (owens, 1980). 

6.8 CRAVEN GROUP (CRAV) 

The Craven Group, of mainly hemipelagic facies, is 

dominated by deposits of calcareous mudstone interbedded 

with limestone and subordinate limestone breccia, 

conglomerate and sandstone. The limestones are typically 

pale coloured and coarsely bioclastic towards the base of 

the group and more argillaceous towards the top. The group 

largely occurs in southern Great Britain (see waters et al., 

2007, for a full description), but it also encroaches upon the 

onshore Northern england province where: 

in south Cumbria and in the Askrigg Block–Craven 

Basin ‘Transition Zone’ it comprises the Bowland shale 

Formation; 

on the Isle of Man it comprises the Hodderense limestone 

and Bowland shale formations. 

Knoll-reef and slope carbonate turbidite facies also occur on 

the southern margin of the Askrigg Block. in south Cumbria 

the upper boundary of the yoredale Group occurs at the 

base of the Cravenoceras leion marine Band, where the 

thinly interbedded limestones, mudstones and subordinate 

sandstones of the Alston Formation pass upward into the 

thick mudstones and fine-grained siltstones of the Bowland 

shale Formation, Craven Group. on the south isle of man, 

the upper boundary of the Great scar limestone Group 

occurs at a change from the wackestones and packstones of 

the Knockrushen Formation to massive lime mudstones with

micrite nodules of the Hodderense limestone Formation (see 

dickson et al., 1987) and at a change from the limestones 

with subordinate claystones and siltstones of the Balladoole 

Formation to the overstepping claystone with detrital carbonates 

of the Bowland shale Formation. The diachronous 

base of the millstone Grit Group (fluvio-deltaic (‘Millstone 

Grit’) facies) defines the top of the Craven Group. 

The type area of the Craven Group is the Craven Basin 

of lancashire (after which it is named) and its main extent 

is across central england and North wales. it is Chadian 

to yeadonian in age and reaches a maximum thickness 

in excess of 5000 m in the widmerpool half-graben (see 

waters et al., 2007). in south Cumbria the group is about 

120 m thick and pendleian in age. in the isle of man it is 

about 264 m thick and Holkerian to late Arnsbergian in age. 

6.8.1 Hodderense Limestone Formation (BOH) 

since the Bowland shale Formation extends into onshore 

southern Great Britain the definition that follows has been 

unified with that of waters et al. (2009). 

Name 

The formation was first recognised informally as the 

Beyrichoceras hodderense Bed (parkinson, 1926). Revision 

of the eponymous fauna to Bollandoceras hodderense led 

to a change in the informal name (earp et al., 1961), which 

was subsequently revised to the Hodderense limestone 

Formation, formally defined by Riley (1990). 

Lithology 

Grey sandstone occurs in the Cow Ark Anticline (wadge et 

al., 1983). Chert is common in the isle of man sections, where 

some beds are multistorey and display lag horizons composed 

of reworked micrite nodules, inadunate crinoids, bellerophontid 

gastropods, cephalopods, trilobites and sponges (Chadwick et 

al., 2001). Also present is the trace fossil Helminthoides. 


The facies represents a deep-marine hemipelagic carbonate, 

deposited in a setting that was mainly starved of clastic 

supply and lay below storm wave base. Helminthoides is a 

deep-water trace fossil. 

Stratotype 

The type section is the east bank of the River Hodder, Great 

Falls [sd 7035 3999], near stonyhurst, near Clitheroe, 

lancashire. The base and top of the formation are seen in 

the section (earp et al., 1961). Reference sections include 

south of the old lime kilns at the visitor Centre at scarlett, 

isle of man [sC 2580 6620] where the base of the formation 

is seen, and a cliff section at scarlett point, isle of man [sC 

2583 6633] where the top of the formation is seen. 


in the Craven Basin the base of the formation is drawn at the 

base of the first cream-coloured wackestone with dark blue 

micritic nodules of the Hodderense limestone Formation, 

where it rests conformably on grey or dark grey mudstone 

and calcisiltite of the Hodder mudstone Formation, Craven 

Group, of Chadian to Holkerian age. 

in the south of the isle of man, at the visitor Centre at 

scarlett, south of the old lime kilns, the wackestones and 

packstones of the underlying Knockrushen Formation are 

overlain by the massive lime mudstones of the Hodderense 

limestone Formation (Figure 8, Column 8). The base of the 

latter is taken at the lowest mottled horizon (dickson et al., 

1987), and this mottling is a result of the presence of blue 

129 

or grey micrite nodules up to 3 cm in size. 

in the Craven Basin, the top of the formation is drawn at 

the conformable upward passage from the highest nodule 

bearing cream-coloured wackestone bed of the Hodderense 

limestone Formation, to the first grey mudstone of the 

pendleside limestone Formation, Craven Group, of late 

Holkerian to Asbian age. 

in the south of the isle of man, at scarlett point [sC 2583 

6633], the upper boundary of the Hodderense limestone 

Formation occurs below the lowest black claystone of the 

wackestones, lime-mudstones and interbedded claystones 

of the scarlett point member, Bowland shale Formation 


Thickness 

up to 15 m in north-west england and 14 m in the isle of 

man. 

Distribution 

Craven Basin, north-west england, although removed 

beneath the unconformity in the skipton area; south isle 

of man. 


Holkerian. The ammonoid assemblage, including 

Bollandoceras hodderense, is indicative of the upper part 

of the Bollandites–Bollandoceras (BB) Zone (Aitkenhead 

et al., 1992). in the south isle of man, scarlett Quarry [sC 

258 662] is the type locality of the ammonoid Merocanites 

henslowi. 

6.8.2 Bowland Shale Formation (BSG) 

since the Bowland shale Formation extends into southern 

Britain the definition that follows has been unified with 

that of waters et al. (2009). information relevant solely to 

northern Britain is, however, provided under the subhead 

‘Local notes’. 

Name 

The Bowland shale Group of earp et al. (1961) was 

subdivided into lower and upper Bowland shale 

formations, the division between the two taken at the base 

of the Cravenoceras leion marine Band. The equivalent 

succession was referred to as the Bowland shale Formation 

by Fewtrell and smith (1980). The formation is formally 

redefined, with the term extended to replace other dark grey 

euxinic shales in North wales (Holywell shales) (davies et 

al., 2004) and the east midlands (edale shales), which were 

in lateral continuity with the deposits of the Craven Basin at 

the time of deposition. 

Lithology 

mainly dark grey fissile and blocky mudstone, weakly 

calcareous with subordinate sequences of interbedded 

limestone and sandstone, fossiliferous in more-or-less 

discrete bands. in the Furness and settle areas the formation 

comprises thick-bedded, blocky to subfissile, dark grey 

and black, organic-rich mudstone, with subordinate beds 

of dark grey siltstone, sandstone and pale brown dolomitic 

limestone. marine bands are also present. The formation 

shows an upwards decrease in carbonate turbidites and a 

concomitant increase in siliciclastic sandstone turbidites 

(see Rose and dunham, 1977; Johnson et al., 2001; 

Arthurton et al., 1988). in the south isle of man, the 

Bowland shale Formation includes black claystone with 

localised deposits of carbonate turbidites, debris flows, 

olistoliths, volcaniclastic deposits and lavas (see Chadwick 



et al., 2001; dickson et al., 1987). At the base of the 

formation, the scarlett point member comprises cherty 

and pyritous tabular beds of pale wackestone and limemudstone 

(dolomitised in places), which display gradational 

boundaries with interbedded black, fissile, blocky claystone. 

The limestone is burrowed and has inadunate crinoidal lags 

and scattered ammonoids. At the top of the formation, 

the scarlett volcanic member is dominated by a series of 

volcaniclastic debris flows and gravity slides. Claystone 

rafts and megaclasts are entrained within the volcaniclastic 

rocks, and carbonate olistoliths and pillow lavas also 

occur. Between the members, where the Bowland shale 

Formation oversteps the Balladoole Formation (Great scar 

limestone Group), coarse-grained detrital carbonates and 

debris beds are common. These include erosively based, 

graded packstone beds, conglomerate, megaclasts and 

large olistoliths (with reef limestone and spectacularly 

preserved ammonoid faunas) derived from the Balladoole 

Formation. The middle part of the exposed part of the 

formation comprises black, calcareous, platy claystone with 

subordinate beds (up to 2 m thick) of dark wackestone, and 

dark detrital packstone debris. in the north isle of man, the 

shellag point Borehole (see below) cored through 27.55 m 

of siltstone, claystone and ironstone. These included two 

marine bands. 


The mudstones accumulated as hemipelagic deposits, 

predominantly from suspension in moderately deep water, 

largely below the storm wave-base. For much of the 

time the water was brackish or fresh and occurred in the 

photic zone (Collinson, 1988). marine bands developed 

during periods of higher salinity when connections with 

the open ocean were established. The thin limestones and 

sandstones were introduced by storms and/or as turbidites; 

the limestones sourced from active carbonate shelves, the 

siliciclastic sediments from active deltas accumulating on 

the margins of the Central pennine Basin. in the south of the 

isle of man, lavas, volcaniclastic debris flows and gravity 

slides are apparently submarine. in the north isle of man, 

the siltstone, claystone and ironstone of the shellag point 

Borehole was mostly of marine origin. 

Stratotype 

Reference sections include: River Ribble at dinckley [sd 

689 366 to 686 366], on the south bank of the River Ribble 

between dinckley Hall and the suspension bridge, about 

400 m to the west downstream (earp et al., 1961); little 

mearley Clough [sd 779 414 to 785 411], 400 to 1100 m 

south-east and upstream from little mearley Hall (earp et 

al., 1961; Fewtrell and smith, 1980); Coed pen-y-maes 

stream section at Holywell [sJ 1939 7650 to 1962 7687] 

(davies et al., 2004); duffield Borehole, near derby 

(BGs Registration Number sK34sw/5) [sK 3428 4217], 

from 335.23 to 405.78 m depth (see Aitkenhead, 1977); 

Roosecote Borehole, Barrow-in-Furness (BGs Registration 

Number sd26Nw/19) [sd 2304 6866], which includes an 

entire thickness of the formation from 491.68 to 613.31 m 

depth (see Rose and dunham, 1977; Johnson et al., 2001); 

shellag point Borehole, north isle of man [NX 4565 9965] 

cored from 100.60 to 128.15 m, but proving neither the base 

nor the top of the formation (Chadwick et al., 2001). 


The conformable base of the formation upon the pendleside 

limestone Formation in the Craven Basin, on the 

widmerpool Formation in the east midlands, on the pentre 

Chert and Cefn-y-Fedw sandstone Formation in North 



130 

wales, and on the Hodderense limestone Formation in the 

south of the isle of man (Figure 8, Column 8), is taken at 

the first appearance of black mudstone above variegated 

mudstones or fine-grained limestones. 

in south Cumbria the lower boundary of the formation 

is taken at the base of the Cravenoceras leion marine Band 

(e1A1), where the dark grey to black marine mudstone 

rests upon thinly interbedded limestones, mudstones and 

subordinate sandstones of the Alston Formation (Figure 9, 

Column 14). 

The Bowland shale Formation onlapped onto, and eventually, 

by the pendleian, extended over the carbonates of 

the Central lancashire High (Trawden limestone Group). 

in the Craven Reef Belt, in the malham Cove–Gordale 

scar area, the fissile mudstones with nodules and thin 

beds of ironstone and limestone of the Bowland shale 

Formation, rest unconformably and diachronously on the 

malham Formation (Great scar limestone Group), or 

yoredale Group (Figure 15, Column 6). 

The top of the formation is taken at the base of the 

millstone Grit Group over most of the pennine Basin 

(Figure 9, Column 14; Figure 15, Column 6) and at the base 

of the morridge Formation in staffordshire and the east 

midlands. The formation shows complex intertongueing 

with the morridge and Cefn-y-Fedw sandstone formations. 

it is seen as a conformable boundary defined by the base of 

the lowermost thick feldspathic sandstone of the millstone 

Grit Group, or quartzitic sandstone of the morridge and 

Cefn-y-Fedw formations, above thick dark grey mudstone 

of the Bowland shale Formation. 

Thickness 

Generally 120–620 m thick. The formation thickens northeastwards 

along the axis of the Central lancashire High, 

from about 22 m in the Roddlesworth Borehole, 68 m 

thick in the Holme Chapel Borehole, and 102 m in the 

Boulsworth Borehole (waters et al., 2009, fig. 11). The 

underlying Trawden limestone Group shows a thinning 

in the same direction (evans and Kirby, 1999), suggesting 

the thickening of the Bowland shale Formation reflects 

available accommodation space. in the Craven Reef Belt 

the Bowland shale Formation is perhaps 30–200 m thick 

(see Arthurton et al., 1988, fig. 22). in south Cumbria, 

the Roosecote Borehole (see above) proved the formation 

to be 121.63 m thick (see Johnson et al., 2001; Rose and 

dunham, 1977). on the isle of man, the Bowland shale 

Formation may be at least 186 m thick; in the north, the 

shellag point Borehole (see above) proved only a part of 

the formation 27.55 m thick. 

Distribution and and regional correlation 

widespread in the Craven Basin (the type area), including 

lancaster, Garstang, settle, Clitheroe, Harrogate districts, 

south Cumbria and the isle of man, but also in North 

wales, staffordshire and the east midlands. The upper part 

of the Bowland shale Formation passes northward into the 

millstone Grit Group and to the south into the morridge 

Formation (waters et al., 2009, fig. 10). 


Asbian to yeadonian. in the type area of the Craven Basin 

the formation ranges from late Asbian (Cf6 Zone) to 

early pendleian (e 1c 1 Zone). The top of the formation 

ranges to younger ages toward the south of the pennine 

Basin, with yeadonian strata present in North wales. 

The Bowland shale Formation of south Cumbria and the 

Craven Reef Belt is pendleian. on the isle of man, the 

formation is Asbian to late Arnsbergian. in the south of

the island, the scarlett point member is of (possibly early) 

Asbian age and includes in the limestone the deep water 

trace fossil Helminthoides sp., and the ammonoid genera 

Beyrichoceras and Bollandoceras. in the north of the 

island, the shellag point Borehole (see above) includes the 

two latest Arnsbergian marine bands with the ammonoid 

Nuculoceras nuculum, an associated shelly fauna and the 

trilobite Paladin. 

Local notes 

in the south isle of man, the Bowland shale Formation 

oversteps the Balladoole Formation along the foreshore 

north-west of salt spring Cottage [sC 244 679], and the 

exposed middle part of the formation is seen for example 

at Black marble Quarry [sC 244 676]. in northern england 

the Bowland shale Formation is ?early Asbian to Namurian 

in age and includes the Emstites leion, Eumorphoceras 

pseudobilingue and C. malhamense marine bands. 


see also Appendix 1. members of the Bowland shale 

Formation in northern Great Britain, in ascending 

stratigraphical order, include: 

6.8.2.1 sCarleTT PoinT MeMBer (sCPT) 

Name 

From scarlett point, isle of man. previous names include 

the scarlett and strandhall Beds (lewis, 1930). The present 

definition is that of Chadwick et al. (2001); (see also 

dickson et al., 1987; lamplugh, 1903). 

Lithology 

The member is characterised by tabular beds of pale 

wackestone and lime-mudstone. These beds, which can be 

cherty and pyritous, have gradational (locally dolomitised) 

boundaries with the subordinate interbedded black fissile, 

blocky claystones. 


deposition was in a deep marine hemipelagic environment, 

but with periodic fine clastic and carbonate supply 

(gravitational). 

Stratotype 

A partial type section is exposed in coastal sections at 

scarlett point [sC 2570 6620 to 2583 6633] where about 

14 m of evenly bedded, pale grey wackestone and limemudstone 

with interbedded black claystone are seen (see 

dickson et al., 1987, pp. 214–217; Chadwick et al., 2001, 

p. 62). 


The base of the member is taken at the lowest black 

claystone (about 0.12 m thick) overlying the fine-grained, 

pale mottled limestone (wackestone) of the Hodderense 

limestone Formation at scarlett point [sC 2583 6633] 


The top of the member is not exposed so the nature of 

the upper boundary is unknown. The overlying succession 

comprises black hemipelagic mudstones of the undivided 

Bowland shale Formation. 

Thickness 

some 14 m. 


southern part of the isle of man, in the Castletown area, 

from scarlett point [sC 2583 6633] north-westwards to 

131 

poyllvaaish [sC 2440 6761]. visean rocks in the northern 

part of the island are entirely concealed so it is unknown 

whether it is present in the north. 


Asbian. Chondritiform and Helminthoides burrows 

are common in the limestones. inadunate crinoid lags 

and scattered ammonoids of genera Beyrichoceras or 

Bollandoceras also occur, some preserved in semi-buoyant 

resting position with the venter resting on the former sea 

bed. 

6.8.2.2 sCarleTT volCaniC MeMBer (sCv) 

Name 

From scarlett point, isle of man. previous names include 

the scarlett volcanic series of lewis (1930) and the 

scarlett volcanic Formation of dickson et al. (1987). The 

present definition is that of Chadwick et al. (2001). see also 

lamplugh (1903). 

Lithology 

The member is dominated by submarine volcaniclastic 

debris flows and gravity slides. olistoliths of older 

Tournaisian and/or visean carbonates and claystone rafts 

also occur, as do isolated vesicular basaltic clasts. 


The tuffs are waterlain, the volcaniclastic debris flows and 

gravity slides are submarine. 

Stratotype 

A partial type section (a strike section through the 

member) comprises largely continuous coastal outcrops 

from scarlett point [sC 2570 6610] to Close-ny-Clollagh 

point [sC 2450 6710]. Here the sharp base of the 

member is succeeded by submarine volcaniclastic rocks 

(including debris flows, gravity slides and pillow lavas) 

with entrained claystone rafts and megaclasts. The section 

is no more than 50 m thick and the top of the member is 

not seen (see dickson et al., 1987, pp. 219–223; Chadwick 

et al., 2001, p. 63). 


The base is clearly seen on the foreshore below Closeny-Chollagh 

point [sC 245 671] where volcaniclastic 

rocks rest with a sharp, baked contact on underlying dark 

claystones of the Bowland shale Formation (Figure 8, 

Column 8). 

The top of the member is not exposed, so the nature of 

the upper boundary is unknown. 

Thickness 

some 50 m. The thickness of the member is difficult to 

estimate due to the numerous olistoliths and rolling dips 

present in the outcrop. 


southern part of the isle of man, in the Castletown area, 

from scarlett point [sC 257 661] to Close-ny-Clollagh point 

[sC 245 671]. visean rocks in the northern part of the island 

are entirely concealed and hence it is unknown whether it is 

present in the north. well 112/19-1, just off the north-east 

of the isle of man proved 198 m of Brigantian to pendleian 

strata and no volcanic successions, so the member is likely 

to be absent in the northern part of the island. 

Age 

Brigantian. 



6.9 MILLSTONE GRIT GROUP (MG) 

The name ‘millstone Grit’ is derived from the familiar 

‘gritstones’ (coarse-grained sandstones) that were used 

historically in flourmills. whitehurst (1778) first proposed 

the lithostratigraphical name ‘millstone Grit’, since when it 

has become chronostratigraphical in concept. synonymous 

with the Namurian, it was divided, in the Central pennine 

Basin, into stages bound by key widespread marine 

bands (see George and wagner, 1972; Ramsbottom et 

al., 1978). The historical precedence was established in 

the Bradford district (stephens et al., 1953) where six 

‘groups’ were defined using ammonoid biozones, which 

broadly correspond to the modern stages of the Namurian. 

The stratigraphical Framework Committee concluded that 

this approach should be maintained, and each of the 

seven Namurian stage successions was assigned a distinct 

formation name, with the exception of the thin, commonly 

mudstone-dominated successions of the Chokierian and 

Alportian, which were joined to form a single formation 

(see waters et al., 2007). where marine bands cannot be 

recognised, or other biostratigraphical data are absent, the 

group is left undivided. 

in central england, the component formations of the 

group, in ascending order, are the (pendleian) pendleton, 

(Arnsbergian) silsden, (Chokierian and Alportian) 

samlesbury, (Kinderscoutian) Hebden, (marsdenian) 

marsden, and (yeadonian) Rossendale formations. They 

are also present in northern england, but limited to the 

Askrigg Block, south Cumbria (the pendleton Formation 

only) and north isle of man (the Rossendale Formation 

only). in northern england (Figure 7), the heterolithic succession 

of grey sandstone, siltstone and mudstone with subordinate 

coal and seatearth is characterised by the commonly 

coarse-grained nature of the sandstone (formerly referred 

to as grit), typically an arkosic or subarkosic arenite. marine 

bands, representing transgressive events, are present in the 

succession, although fewer in number than the comparable 

succession in the Central pennine Basin. The marine bands 

consist typically of dark grey to black, calcareous, shaly 

mudstone about 0.5 m thick. distinct ammonoid faunas and 

the extensive correlation of the marine bands make them of 

primary stratigraphical importance. 

in Britain, the millstone Grit Group was deposited by 

repeated progradation of deltas, predominantly from the 

north and east. delta-top subfacies are characterised by condensed, 

predominantly upward-fining cycles of sandstone 

to structureless clayrock. Thick, high-alumina seatclay, 

fireclay and bauxitic clay are common, with sporadic beds 

of limestone, ironstone, cannel and coal. This sub-facies 

is more typical of the succession developed in northern 

england, north of the Craven Fault system. it is probable 

that many of the sandbodies are linear in geometry and 

occupy incised valleys, with well-developed palaeosols 

developed on the interfluves. sheet-like and laterally extensive 

deltaic sandbodies, upward-coarsening with a lower 

part dominated by mouth-bar deposits overlain by distributary 

sands, more typical of the late Namurian succession 

of the Central pennine Basin may extend onto the southern 

margin of the Askrigg Block. deep-water deltaic sequences 

deposited in a delta-front apron of coalescing turbidite 

lobes, a feature of the lower part of the group in the Central 

pennine Basin, are absent north of the Craven Fault system. 

The base of the millstone Grit Group on the Askrigg 

Block is taken at the base of the ‘Bearing’ or Howgate 

edge grits, pendleton Formation. Here, the mixed shelf carbonate 

and deltaic succession of the underlying stainmore 

Formation, yoredale Group is succeeded, at an unconform- 



132 

ity of e1c age, by sandstone-dominated strata (see Brandon 

et al., 1995). The base of the group in south Cumbria is 

taken at the diachronous base of the pendleton Formation, 

where the mudstone-dominated succession of the underlying 

Bowland shale Formation, Craven Group, gives way to 

a predominantly feldspathic sandstone succession. The base 

of the group on the north isle of man in the Ballavaarkish 

(shellag North) Borehole [NX 4625 0070] appears to be 

within the Rossendale Formation at 164.55 m depth. This 

is at the base of listricated claystone that may lie in the 

upper part of the Cancelloceras cumbriense marine Band 

(see Chadwick et al., 2001). This position lies immediately 

above faulted strata that comprise thin-bedded, listricated 

and shattered black claystone and siltstone, and pale finegrained 

sandstone to a depth of 172.34 m. Below this 

level occurs a sequence of massive dolostones apparently 

assigned to either the Great scar limestone Group or the 

yoredale Group by Chadwick et al. (2001). The base of 

the pennine Coal measures Group (fluviodeltaic (‘Coal 

Measures’) facies) defines the top of the millstone Grit 

Group. 

The thickest development of the millstone Grit Group is 

in the northern part of the Central pennine sub-basin, where 

1225 m is recorded in wharfedale (Ramsbottom, 1978). 

As the Namurian succession passes northwards over the 

Askrigg Block it becomes significantly reduced in thickness 

to about 400 m in the Colsterdale–upper Nidderdale 

area (dunham and wilson, 1985), and the presence of a 

mid Carboniferous unconformity is indicated here by the 

absence of Alportian strata (Ramsbottom, 1977a). The 

millstone Grit Group is represented on the north isle of man 

in the Ballavaarkish (shellag North) Borehole (see above) 

solely by the Rossendale Formation. it is at least 26 m thick 

and yeadonian in age (see Chadwick et al. 2001). 

since the millstone Grit Group extends into southern 

Britain the definitions that follow for the constituent formations 

have been unified with those of waters et al. (2009). 

information relevant solely to northern Britain is, however, 

provided under the subhead ‘Local notes’. 

6.9.1 Pendleton Formation (PENDL) 

Name 

The new name pendleton Formation is proposed to identify 

all millstone Grit Group strata of pendleian age. pendleton 

Formation supersedes previous terms such as pendle 

Grit Formation and Brennand Grit Formation, used in 

the lancaster district for components of the pendleton 

Formation (Brandon et al., 1998). The formation coincides 

with the skipton moor Grits of the Bradford district, 

defined by stephens et al. (1953). 

Lithology 

Fine- to very coarse-grained and pebbly, feldspathic 

sandstone, interbedded with grey siltstone and mudstone, 

with subordinate marine black shales, thin coals and 

seatearths. 


during the pendleian the fluvial succession of the ‘Bearing 

Grit’ crossed the Askrigg Block occupying an incised 

valley (waters et al., 2009, fig. 10). on reaching the 

Craven Fault system the marked slope into the Central 

pennine sub-basin resulted in deep-water turbidite-fronted 

deltas prograding into the northern part of the sub-basin, 

forming the pendle Grit member. The deposits typically 

comprise background sedimentation of thinly interbedded 

silty mudstones, siltstones and fine-grained sandstones

deposited on the submarine prodelta slope. These are cut 

by massive, laterally impersistent, coarse-grained, pebbly 

sandstones filling turbidite channels (Aitkenhead et al., 

2002). The great thickness of sediments was sufficient to 

infill the northern part of the basin by late pendleian times 

and allow the shallow-water fluviodeltaic coarse-grained, 

cross-bedded successions of the warley wise Grit to extend 

several kilometres southwards into the basin. 

Stratotype 

partial type sections occur at pendleton moor on the west 

flank of pendle Hill between light Clough [sd 7516 

3764] (the basal stratotype for the pendleian stage) and 

the excellent section at mearley Clough [sd 785 411] 

where the base of the formation is exposed (earp et al., 

1961). At Faugh’s delph [sd 820 392], the upper part of 

the formation is exposed with about 30 m of very coarsegrained, 

massive sandstone of the warley wise Grit (earp 

et al., 1961). 


The base of the formation is taken at the base of the first 

thick quartz-feldspathic sandstone of pendleian age, present 

above the dark grey, carbonaceous, fissile mudstone of the 

Bowland shale Formation, which in the north lancashire 

area and Bradford–Harrogate districts, is at the base of the 

pendle Grit member, and on the Askrigg Block, is taken at an 

unconformity of e1c age at the base of the ‘Bearing’ or lower 

Howgate edge Grit (Brandon et al., 1995), overlying the 

mixed shelf carbonate and deltaic succession of the yoredale 

Group (Figure 9, Column 17). The base is taken at the point in 

the sequence where sandstone becomes predominant. 

The top of the formation occurs at the sharp conformable 

base of the dark grey, fissile mudstone of the Cravenoceras 

cowlingense marine Band (e2A1) with eponymous fauna, 

which is commonly underlain by a thin, fine-grained, calcareous 

and phosphatic sandstone of the pendleton Formation 

(Figure 9, Column 17; Figure 15, Column 5). locally, in 

the absence of the Cravenoceras cowlingense marine Band, 

the top of the formation is taken at the top of the warley 

wise Grit (north lancashire area and Bradford–Harrogate 

districts), the base of the mirk Fell ironstones (stainmore 

Trough) (Figure 15, Column 2) or the top of the lower 

Howgate edge Grit (northern part of the Askrigg Block). 

Thickness 

lancaster 800 m; Bradford 600 m; southern part of the 

Askrigg Block up to 45 m thick with a condensed succession. 

About 30 m thickness is present in the Great shunner 

Fell area (Figure 15, Column 3), where the formation is 

dominated by the lower Howgate edge Grit. 


The Craven Basin of north lancashire and north yorkshire 

between lancaster [sd 47 61], pendle Hill [sd 80 41], 

skipton moor [se 00 50] and Harrogate [se 30 55], and also 

present across the southern part of the Askrigg Block, and in 

the masham district [se 29] (dunham and wilson, 1985). 

The formation passes southward into basinal mudstones of 

the Bowland shale Formation (Craven Group). 


pendleian (e 1 ). The top of the formation is defined at the base 

of the Cravenoceras cowlingense (e 2a ) Ammonoid Zone. 

Local notes 

within the southern part of the Askrigg Block the formation 

is dominated by two sandstones, the ‘Bearing Grit’ and 

133 

overlying underset (or Top) Grit. These sandstones pass 

southwards respectively into the thick turbiditic succession 

of the pendle Grit member (pG) (Figure 15, Column 6) (of 

thinly interbedded silty mudstone, siltstone and fine-grained 

sandstone, cut by massive, laterally impersistent, coarsegrained, 

pebbly sandstones) and the warley wise Grit (of 

coarse-grained, cross-bedded sandstone) (see Brandon et 

al., 1995). in the Great shunner Fell area, a condensed 

succession is dominated by the lower Howgate edge 

Grit (dunham and wilson, 1985). within the stainmore 

Trough, the mirk Fell Ganister (mKFG) occurs at the same 

stratigraphical level as the lower Howgate edge Grit of the 

Askrigg Block (Figure 15, Column 2). 

6.9.2 Silsden Formation (SILS) 

Name 

The new name silsden Formation is proposed to identify all 

millstone Grit Group strata of Arnsbergian age. silsden was 

chosen as the name had been used in the Bradford district 

for the silsden moor Grit Group (stephens et al., 1953). 

The base of the silsden moor Grit Group was defined at 

the base of the Cravenoceras cowlingense (e2a ) marine 

Band, but the top of the group was taken as the base of the 

Nuculoceras nuculum (e2c ) marine Band, resulting in part 

of the Arnsbergian succession falling within the overlying 

middleton Grit. The newly defined formation is named 

after silsden village [se 040 470], to distinguish it from the 

silsden moor Grit Group, named after the upland area to 

the west of silsden. silsden Formation supersedes previous 

terms such as Roeburndale, ward’s stone sandstone, Caton 

shale, Claughton, silver Hills sandstone and Crossdale 

mudstone formations, used in the lancaster district for 

components of the silsden Formation (Brandon et al., 1998). 

Lithology 

Fine- to very coarse-grained pebbly feldspathic sandstone, 

interbedded with grey siltstone and mudstone and 

subordinate marine black shales, thin coals and seatearths. 

The lower part of the formation is dominated by thinly 

bedded sandstone, siltstone and mudstone forming sharpbased, 

normal graded beds interpreted to be of turbiditic 

origin. 


The succession is dominated by a great thickness of turbiditic 

siltstones and thin sandstones with periodic progradation of 

shallow-water lobate deltas about 10–15 km south into the 

Central pennine Basin (waters, 1999). 

Stratotype 

Basal exposures at lister Gill [se 0091 4946], overlain 

by interbedded turbiditic sandstone, micaceous mudstone, 

marchup Grit, and by dark grey fossiliferous mudstones of 

the Eumorphoceras yatesae and Cravenoceras edalensis 

marine bands occur along Bracken Hill Gill [se 0304 4686 

to 0324 4697] (Addison, 1997). 


The base is taken at a sharp base of dark grey fissile 

claystones of the Cravenoceras cowlingense marine Band 

(e2A1) with a diagnostic eponymous fauna, commonly 

underlain by a thin, fine-grained, calcareous and phosphatic 

sandstone of the pendleton Formation (Figure 9, Column 17; 

Figure 15, Column 5). elsewhere the boundary is taken at 

the base of the first thick quartz-feldspathic sandstone of 

Arnsbergian age, present above the dark grey, carbonaceous 

mudstone of the Bowland shale Formation. it is taken at the 



ase of the mirk Fell ironstones in the stainmore Trough 

(Figure 15, Column 2) or the top of the lower Howgate 

edge Grit in the northern part of the Askrigg Block. 

The top of the formation is taken at the base of the dark 

grey fissile claystones of the Isohomoceras subglobosum 

marine Band (ismB), with a diagnostic eponymous fauna 

(Figure 9, Column 17; Figure 15, Column 5). where the 

marine band is not proven, the boundary is taken at the 

base of a thick, mid or dark grey mudstone succession, with 

numerous marine bands of the samlesbury Formation. it is 

taken at the top of the lower Follifoot Grit in the southern 

part of the Askrigg Block, or the base of a mudstone succession 

with Lingula in the stainmore Trough. 

Thickness 

lancaster 1000 m; Bradford 400 m; Askrigg Block and 

stainmore Trough up to 190 m. 


Craven Basin of north lancashire and north yorkshire, 


skipton moor [se 00 50] and Harrogate [se 30 55]. Also 

present across the southern part of the Askrigg Block, 

masham district [se 29] (dunham and wilson, 1985). The 

formation passes southward into basinal mudstones of the 

Bowland shale Formation (Craven Group). 


Arnsbergian (e 2 ). The base is taken at the base of the 

Cravenoceras cowlingense marine Band, and the top at the 

base of the lowermost Isohomoceras subglobosum marine 

Band. 

Local notes 

laterally impersistent cross-bedded sandstones are present 

along the northern margin of the Central pennine sub-basin. 

within the southern part of the Askrigg Block, the lower 

part of the formation is dominated by the Nidderdale shales, 

comprising mudstones with common Sanguinolites bands 

(wilson, 1977; dunham and wilson, 1985; Brandon et al., 

1995). in the western part of the Askrigg Block a lenticular 

sandstone, the upper Howgate edge Grit, occurs towards 

the base of the formation. in the northern part of the Askrigg 

Block and stainmore Trough, sandstones (for example, 

the Fossil sandstone and High wood Grit), ganisters (for 

example, the Kettlepot Ganister), and thin limestones (for 

example, the lad Gill limestone) occur interbedded with 

mudstones at this stratigraphical level (Figure 15, Columns 

2, 3). The middle part of the formation is dominated by the 

Red scar Grit (southern Askrigg Block), pickersett edge Grit 

(northern Askrigg Block) and High wood Grit (stainmore 

Trough). These sandstones are typically overlain by a 

marine succession (the Colsterdale, shunner Fell (Figure 

15, Column 3), water Crag (Figure 15, Column 2) and 

High wood marine bands), which in the southern part of the 

Askrigg Block are known as the ‘Colsterdale marine Beds’. 

These are overlain by a mudstone, siltstone and sandstone 

succession (the scar House Beds of wilson, 1977), which, 

in turn, are overlain by the lower Follifoot Grit. 

Brandon et al. (1995) postulated the presence of 

an intra-e 2a 3 unconformity at the base of the Red 

scar Grit. The Colsterdale marine Beds comprise the 

Eumorphoceras yatesae (e 2a 3), Cravenoceratoides 

edalensis (e 2b 1) and Cravenoceratoides nitidus (e 2b 2) 

marine bands (Cooper and Burgess, 1993). The lower 

Follifoot Grit is known to be Arnsbergian in age as it is 

immediately overlain by the Nuculoceras nuculum (e 2c ) 

marine Band (wilson, 1977). 



134 

6.9.3 Samlesbury Formation (SAML) 

Name 

The new name samlesbury Formation is proposed to 

identify all millstone Grit Group strata of Chokierian and 

Alportian age. The term middleton Grit Group of Bradford 

(stephens et al., 1953) is unsuitable as there is a sandstone 

already called middleton Grit, and it is Arnsbergian in 

age. The new name was chosen from samlesbury Bottoms 

[sd 618 291] where a complete basinal succession in the 

Chokierian and Alportian is exposed. 

Lithology 

dark grey mudstone, common thin shaly mudstones, 

subordinate sandstone and siltstone, and locally, in the 

Bradford area, a thick, coarse-grained, cross-bedded 

sandstone (the Brocka Bank Grit) (waters, 1999). 


during the Chokierian and Alportian there appears to be 

little clastic input into the pennine Basin. The succession 

is condensed with some hemipelagic marine shales. A 

shallow-water lobate delta, the Brocka Bank Grit prograded 

about 15 km into the Harrogate sub-basin (waters, 1999). 

Stratotype 

The type section is a composite section in the River darwin 

at samlesbury Bottoms [sd 618 291]. This shows dark grey 

mudstones and common marine shales, including the marine 

bands that define the base and top of the formation (moore, 

1930; price et al., 1963). stonehead Beck, Cowling, North 

yorkshire [sd 9473 4330], shows a continuously exposed 

40 m succession including the base Chokierian stratotype. 

This equates to the base of the samlesbury Formation, and 

defines the position of the mid Carboniferous boundary 

(Riley et al., 1995). 


The sharply conformable base of the formation is taken at the 

base of the dark grey shaly mudstone of the Isohomoceras 

subglobosum marine Band with an eponymous fauna, 

where the formation overlies the interbedded sandstone, 

siltstone and mudstone succession of the silsden Formation 

(Figure 9, Column 17; Figure 15, Column 5). where the 

marine band is absent from the interval, the base of the 

formation is taken at the top of the lower Follifoot Grit 

in the southern part of the Askrigg Block, or at the base 

of a mudstone succession with Lingula in the stainmore 

Trough. in the southern part of the Central pennine Basin, 

the boundary is taken at the base of the first thick quartzfeldspathic 

sandstone of Chokierian to Alportian age that is 

present above the Bowland shale Formation. 

The top is taken at the sharp conformable base of the 

dark grey shaly mudstone of the Hodsonites magistrorum 

marine Band, including an eponymous fauna, overlain 

by the siltstone-dominated lower part of the Hebden 

Formation. The marine band is underlain by the mudstonedominated 

succession of the samlesbury Formation. where 

the marine band is absent from the interval, the top of the 

formation equates with the base of the Cayton Gill shale 

in the south of the Askrigg Block (wilson, 1977) and the 

base of the mousegill marine Beds in the stainmore Trough 

(owens and Burgess, 1965). 

Thickness 

in lancashire there are 58 m of Chokierian and 6 m of 

Alportian strata, entirely within shaly mudstones (Brandon 

et al., 1998). in Bradford the succession including the

Brocka Bank Grit is 75 m thick (waters, 1999). The 

formation is less than 30 m thick along the southern part of 

the Askrigg Block, and in the stainmore Trough, the thin 

Chokierian succession is no more than 20 m thick. 


The Craven Basin of north lancashire and north yorkshire, 


skipton moor [se 00 50] and Harrogate [se 30 55] and 

the southern part of the Askrigg Block and the stainmore 

Trough. The formation passes southward into basinal 

mudstones of the Bowland shale Formation (Craven 

Group). 


Chokierian to Alportian (H 1 –H 2 ). part or all of the 

Alportian succession may be missing regionally due to a 

mid Carboniferous unconformity (Riley et al., 1995). The 

Isohomoceras subglobosum marine Band occurs at the 

base of the formation, and the top is taken at the base of the 

Hodsonites magistrorum marine Band (R 1a ). 

Local notes 

Along the southern part of the Askrigg Block, the formation 

comprises a lower mudstone-dominated Follifoot shale, 

overlain by the upper Follifoot Grit (wilson, 1977; dunham 

and wilson, 1985). unlike in the Craven Basin to the south, 

no strata of Alportian age have been proved in the Askrigg 

Block and stainmore Trough (Ramsbottom et al., 1978). 

in the stainmore Trough, a thin Chokierian succession is 

postulated from miospore evidence (owens and Burgess, 

1965). A non-sequence is considered to be present above 

the upper Follifoot Grit. 

6.9.4 Hebden Formation (HEBD) 

Name 

The new name Hebden Formation is proposed to identify 

all millstone Grit Group strata of Kinderscoutian age. The 

term Kinderscout Grit Group of Bradford (stephens et al., 

1953) is unsuitable as there is a sandstone already called 

Kinderscout Grit, and the name has also been used for the 

stage. The new name was chosen from Hebden Bridge 

[sd 990 270] and Hebden water, which provide excellent 

sections representative of much of the Kinderscoutian 

succession. The basal marine band has, however, not been 

found within this area. 

Lithology 

Fine- to very coarse-grained and pebbly, feldspathic 

sandstone interbedded with grey siltstone and mudstone, 

with subordinate marine black shales, thin coals and 

seatearths. The lower part of the formation is dominated by 

a turbiditic facies of thinly interbedded siltstone and finegrained 

sandstone with laterally impersistent and locally 

thick, massive, coarse- to very coarse-grained sandstones. 

The upper part of the formation is dominated by sheet-like 

laterally persistent, cross-bedded sandstones, interbedded 

with siltstone and mudstone; Coal and seatearth are largely 

restricted to the upper part of the formation. A distinctive 

feature of the lower part of the formation within the Askrigg 

Block succession is the presence of brachiopod-bearing 

sandstones, the Cayton Gill shell Bed and ure shell Bed 

(wilson and Thompson, 1965; wilson, 1977). 


during the early Kinderscoutian there is a return to 

deposition in deep-water deltaic successions in the northern 

135 

part of the basin. in wharfedale this is dominated by 125 m 

of mostly delta slope siltstones with possible turbidite 

feeder channels, the Addlethorpe Grit. This marks the 

initiation of a major deltaic advance with the distributary 

channel sandstones of the Addingham edge Grit, 15–55 m 

thick prograding over the delta slope deposits. The delta 

system appears to be thickest in the pennines, thinning 

westwards into lancashire. in the south of the basin, where 

hemipelagic shales had continued to be deposited until 

Kinderscoutian times, the greater accommodation space 

resulted in a marked southward thickening of the deltaic 

succession to about 600 m in north derbyshire. Here, the 

onset of deltaic sedimentation is marked by the thin-bedded 

distal turbidites of the mam Tor sandstone (Allen, 1960). 

This passes up into the very thick-bedded, more erosional 

turbidites of the shale Grit (walker, 1966). The overlying 

Grindslow shales represent the delta-slope deposits and 

the lower Kinderscout Grit represents fluvial distributary 

channels (Collinson, 1969; mcCabe, 1978; Hampson, 1997). 

The general southward progradation of deltas resulted in the 

youngest Kinderscoutian sandstone, the upper Kinderscout 

Grit, extending furthest south. in the Goyt Trough the 

longnor sandstone, a turbiditic sandstone equivalent to the 

upper Kinderscout Grit, marks the base of the millstone 

Grit Group. Heavy mineral studies have demonstrated the 

northerly provenance of the Addingham edge Grit (Cliff et 

al., 1991) and Kinderscout Grit (Chisholm and Hallsworth, 

2005). sporadic marine environments are evidenced by the 

presence of subordinate marine black mudstones, and in 

the Askrigg Block the presence of the brachiopod-bearing 

sandstones, the Cayton Gill shell Bed and ure shell Bed. 

Stratotypes 

partial type sections include Crimsworth dean, north of 

Hebden Bridge [sd 9899 3079 to 9926 3141], which 

shows the upper boundary with the marsden Formation 

as a transition from the underlying turbiditic facies to the 

overlying fluvial sheet sandstone facies (stephens et al., 

1953; davies and mclean, 1996); and Blackden Brook, 

Kinder scout, derbyshire [sK 1223 8842 to 1171 8833], 

which provides an excellent stream section 150 m thick 

of the shale Grit, Grindslow shales and the base of the 

Kinderscout Grit (stevenson and Gaunt, 1971; davies and 

mclean, 1996). 


The base of the formation is taken at the base of the dark 

grey, shaly mudstone Hodsonites magistrorum marine Band 

with an eponymous fauna, where the formation overlies the 

mudstone-dominated samlesbury Formation. elsewhere, 

where this marine band has not been found (Figure 15, 

Column 5), the base of the formation equates with the base 

of the Cayton Gill shale in the south of the Askrigg Block 

(wilson, 1977) and the base of the mousegill marine Beds 

in the stainmore Trough (owens and Burgess, 1965). in 

the south of the Central pennine Basin the base is taken 

at the base of the first thick quartz-feldspathic sandstone 

of Kinderscoutian age, present above the Bowland shale 

Formation. 

The top is taken at the sharp conformable base of the 

dark grey, shaly mudstone of the Bilinguites gracilis marine 

Band with an eponymous fauna, typically overlain by mudstone 

of the marsden Formation. The marine band is underlain 

by sandstone including the upper Kinderscout Grit of 

the Hebden Formation. elsewhere, where the marine band 

is absent, in the Askrigg Block the base of the formation 

is taken at the base of the wandley Gill shale, described 

by wilson and Thompson (1965) as 3 m of shale with a 



Lingula-band at the base, overlying a seatearth at the top 

of the upper Brimham Grit. in the stainmore Trough the 

base of the marsden Formation is taken at the base of a 

6 m-thick shale with Productus carbonarius, which overlies 

a 0.15 m-thick shaly coal (owens and Burgess, 1965). 

Thickness 

preston 335 m; Bradford 275 m; derbyshire 600 m; 

southern part of the Askrigg Block about 100 m; stainmore 

Trough 40 m. 


North lancashire and north yorkshire, between lancaster 

[sd 47 61] and Harrogate [se 30 55], extending southward 

to north derbyshire [sK18] and on the Askrigg Block 

and stainmore Trough. The formation passes southward 

into basinal mudstones of the Bowland shale Formation 

(Craven Group). 


Kinderscoutian (R 1a ). The base is taken at the base of the 

Hodsonites magistrorum marine Band (R 1a ) and the top at 

the base of the Bilinguites gracilis marine Band (R 2a ). 

Local notes 

marine shales of the R 1a Zone (equivalents of the mousegill 

marine Beds of the stainmore Trough) occur within the 

Cayton Gill shale of the southern part of the Askrigg Block 

(see owens and Burgess, 1965; wilson, 1977). Thick 

sandstones present in the Askrigg Block area include the 

libishaw sandstone and the lower and upper Brimham 

Grits. 

6.9.5 Marsden Formation (MARSD) 

Name 

The new name marsden Formation is proposed to identify 

all millstone Grit Group strata of marsdenian age. The 

marsden Formation is equivalent to the former middle 

Grit Group of Bradford (stephens et al., 1953), a term 

considered unsuitable. The new name was chosen from 

marsden [sd 030 124], which provides excellent sections 

representative of much of the lower part of the marsdenian 

succession, and is also the location of the basal stage 

stratotype (Ramsbottom, 1981). 

Lithology 

Fine- to very coarse-grained and pebbly feldspathic 


and subordinate marine black shales, thin coals and 

seatearths. 


during the marsdenian, shallow-water deltas dominated, 

extending by late marsdenian times across the entire 

pennine Basin. early marsdenian deltas, including that 

associated with the east Carlton Grit in yorkshire and 

Alum Crag Grit in lancashire, infilled the basin following 

the major transgression associated with the Bilinguites 

gracilis marine Band. These deltas are relatively elongate 

in the flow direction, generally towards the south and show 

evidence of gravity-flow sedimentation in the delta-fronts 

(wignall and maynard, 1996). later deltas are laterally 

persistent sheet sand bodies. in the Goyt and widmerpool 

troughs the turbidite-fronted deep-water deltaic successions 

of the Roaches and Ashover grits show a palaeocurrent 

towards the north-west, but have typical northerly sourced 

petrography (Jones and Chisholm, 1997). These systems 



136 

appear to infill the widmerpool Trough, flowing along the 

axis of the trough. up to 600 m of marsdenian strata are 

recorded between preston and macclesfield (Collinson et 

al., 1977) infilling the accommodation space to the south 

and west of the thick Kinderscoutian succession. Heavy 

mineral studies have demonstrated the northerly provenance 

of the Ashover Grit and Chatsworth Grit (Chisholm and 

Hallsworth, 2005). 

Stratotype 

The partial type section is a stream section at park Clough, 

Hey Green near marsden, west yorkshire [se 0299 1246], 

where 20 m of dark grey mudstone from the lower part of 

the marsden Formation includes the Bilinguites gracilis 

marine Band, above 15 m of cross-bedded sandstone of the 

Hebden Formation (Ramsbottom, 1981). 


The sharp conformable base of the formation is taken at 

the base of the dark grey fissile mudstone of the Bilinguites 

gracilis marine Band, with eponymous fauna where the 

formation overlies the Hebden Formation. in the southern 

part of the Askrigg Block (Figure 15, Column 5), where the 

marine band is absent, the base of the formation is taken at 

the base of the wandley Gill shale, described by wilson 

and Thompson (1965) as 3 m of shale with a Lingula band 

at the base, overlying a seatearth at the top of the upper 

Brimham Grit. in the stainmore Trough the base of the 

formation is taken at the base of a 6 m-thick shale with 

Productus carbonarius, which overlies a 0.15 m-thick shaly 

coal (owens and Burgess, 1965). in the southern part of the 

Central pennine Basin the base of the formation is taken 

at the base the first thick quartz-feldspathic sandstone of 

marsdenian age present above the Bowland shale Formation. 

The top of the formation is taken at the sharp conformable 

base of the dark grey, fissile mudstone of the Cancelloceras 

cancellatum marine Band (G1A1) with eponymous fauna, 

overlain by a dark grey mudstone-dominated succession 

in the lower part of the Rossendale Formation (Figure 9, 

Column 17; Figure 15, Column 5). in the stainmore Trough, 

the equivalent of this marine band, but lacking the diagnostic 

ammonoid fauna, was referred to as the swinstone Bottom 

marine Band (owens and Burgess, 1965). 

Thickness 

up to 600 m thick between preston and macclesfield; 

Bradford 275 m; north derbyshire 450 m; 15 m thick in the 

Kirkby malzeard area of the Askrigg Block; 40 m thick in 

the stainmore Trough. 

Distribution 

lancashire and west yorkshire between lancaster [sd 

47 61] and Harrogate [se 30 55], extending southward to 

north staffordshire [sK 06], and the Askrigg Block and 



marsdenian (R 2 ). The base of the formation is taken at the 

base of the Bilinguites gracilis marine Band and the top at the 

base of the Cancelloceras cancellatum marine Band (G 1a ). 

Local notes 

in both the Askrigg Block and stainmore Trough areas the 

succession comprises a lower mudstone-dominated and 

upper sandstone-dominated unit. on the Askrigg Block 

the former unit is referred to as the wandley Gill shale 

(see wilson and Thompson, 1965) and the latter unit as the 

wandley Gill sandstone (see Ramsbottom et al., 1978).

6.9.6 Rossendale Formation (ROSSE) 

Name 

The new name Rossendale Formation is proposed to 

identify all millstone Grit Group strata of yeadonian age. 

The Rossendale Formation is equivalent to the former 

Rough Rock Grit Group of Bradford (stephens et al., 1953), 

a term considered unsuitable as there is also a Rough Rock 

and Rough Rock Flags for individual sandstones within the 

formation. The new name was chosen from the Forest of 

Rossendale [sd 80 20]. 

Lithology 

A fine- to very coarse-grained and pebbly, feldspathic 


and subordinate marine black shales, thin coals and 

seatearths. Typically, the formation comprises a lower 

mudstone-dominated succession including two prominent 

marine shales, the Cancelloceras cancellatum (G1A1) 

and Cancelloceras cumbriense (G1B1) marine bands, and 

an upper sandstone-dominated succession, including the 

Rough Rock and Rough Rock Flags. 


during the early yeadonian a thick succession of dark 

mudstones was associated with two widespread marine 

transgressions, evident as the Cancelloceras cancellatum 

and Cancelloceras cumbriense marine bands. small 

contributions of sediment from the west are recognised in 

yeadonian times with the upper and lower Haslingden 

Flags of lancashire. These are interpreted as deposits 

within a birdsfoot delta (Collinson and Banks, 1975). 

mclean and Chisholm (1996) showed this westerly source 

of sediment became more important and extensive during 

the westphalian. The upper part of the succession is 

dominated by the sheet-sandstone of the Rough Rock. 

The sandstone is typically very coarse-grained and up to 

45 m thick. it was deposited from braided river channels 

generally flowing towards the south-west (Bristow, 1988). 

Heavy-mineral studies have demonstrated the northerly 

provenance of the Rough Rock (Cliff et al., 1991), but with 

intermixing from a southerly source in the proximity of the 

wales–Brabant massif (Chisholm and Hallsworth, 2005). 

Stratotype 

The type area is the Forest of Rossendale [sd 80 20] 

which provides excellent sections, representative of much 

of the succession including the sandstone of the western 

(Haslingden Flags) and northern provenance (Rough Rock), 

as well as a good exposure of the basal marine band (wright 

et al., 1927). Reference sections include the orchard Farm 

stream section, south-west of Buxton [sK 0226 6903] 

which is the stage stratotype for the yeadonian, with 

both the Cancelloceras cancellatum and Cancelloceras 

cumbriense marine bands present within a section about 

17 m thick (Ramsbottom, 1981). elland Bypass (A629) 

roadcut, near Halifax [se 103 215] provides a 500 m long 

and up to 30 m high section in the Rough Rock and Rough 

Rock Flags (Bristow and myers, 1989). The BGs winksley 

Borehole (BGs Registration Number se27se/9) [se 2507 

7150], in the southern part of the Askrigg Block, includes 

the Rossendale Formation from about 29.7 to 55.89 m depth 

(Cooper and Burgess, 1993). The Ballavaarkish (shellag 

North) Borehole [NX 4625 0070], north isle of man 

includes the Rossendale Formation from 138.4 to 164.55 

m depth, including a 7 m thick, fine- to coarse-grained, 

cross-bedded, feldspathic sandstone contemporaneous with 

(though mineralogically and apparently provincially distinct 

137 

from) the Rough Rock of the pennine Basin. Also occurring 

are palaeosols and listric claystones, one of which, near the 

base of the formation, may include the upper part of the 

Cancelloceras cumbriense marine Band (Chadwick et al., 

2001). 


The sharp conformable base of the formation is taken at the 

base of the dark grey, fissile mudstone of the Cancelloceras 

cancellatum marine Band with an eponymous fauna, where 

the formation overlies the marsden Formation (Figure 9, 

Column 17; Figure 15, Column 5). it typically overlies 

quartz-feldspathic sandstone of the Huddersfield white 

Rock (yorkshire), Holcombe Brook Grit (lancashire), 

Chatsworth Grit (derbyshire). 

The top of the formation is taken at the sharp conformable 

base of the dark grey, fissile mudstone of the subcrenatum 

marine Band (sBmB) with an eponymous fauna present at 

the base of the pennine Coal measures Group. Typically, 

the marine band rests upon coarse- or very coarse-grained 

and pebbly sandstone of the Rough Rock. 

Thickness 

Rochdale (Rossendale) 130 m; Bradford and north 

derbyshire 75 m; stainmore Trough and Askrigg Block 

45 m; north isle of man 26 m. 


The formation occurs in the Central pennine Basin from 

lancashire and west yorkshire, between lancaster [sd 

47 61] and Harrogate [se 30 55], extending southward to 

north staffordshire [sK 06], the Askrigg Block [se 10 80] 

and stainmore Trough [sd 85 15], and locally on the north 

of the isle of man [NX 46 00]. 


yeadonian (G 1 ).The base of the formation is taken at the 

base of the Cancelloceras cancellatum marine Band and the 

top at the base of the subcrenatum marine Band. 

Local notes 

in the stainmore Trough, the equivalent of the Cancelloceras 

cancellatum marine band lacks the diagnostic ammonoid 

fauna and was referred to as the swinstone Bottom marine 

Band by owens and Burgess (1965). The subcrenatum 

marine Band (at the base of the pennine Coal measures 

Group), has not been proved across most of northern 

Great Britain. However, the swinstone Top marine Band 

of owens and Burgess (1965) and a Lingula-band proved 

in the BGs winksley Borehole (see above) (Figure 9, 

Column 17) probably equate with it. on the north isle of 

man the top of the formation in the Ballavaarkish (shellag 

North) Borehole (see above) occurs where the fine- to 

coarse-grained, cross-bedded, feldspathic sandstones of 

the Rossendale Formation (Figure 8, Column 9) are 

superseded by palaeosol and dark grey to black claystone, 

including sporadic fossils in the subcrenatum marine 

Band (sBmB). 

6.10 PENNINE COAL MEASURES GROUP (PCM) 

The ‘Coal measures’ have historically had a chronostratigraphical 

name synonymous with westphalian plus 

stephanian strata. However, the name has recently been 

redefined lithostratigraphically, to describe the main body 

of coal-bearing strata in the westphalian succession (powell 

et al., 2000). 



The pennine Coal measures Group (fluviodeltaic (‘Coal 

Measures’) facies) (Figure 7) extends from the wales– 

Brabant massif northwards to the southern uplands and 

Cumbria (see waters et al., 2007; waters et al., 2009). it 

also occurs in the north isle of man. The group has been 

given the epithet ‘pennine’ to distinguish these coal measures 

from those present in central scotland, and from those 

south of the wales–Brabant massif. The group is subdivided 

stratigraphically into three formations, the lower, middle 

and upper Coal measures, as defined by stubblefield and 

Trotter (1957), and it comprises 10 m-scale cyclothems 

(more numerous than in the millstone Grit) of alternating 

sandstone, grey siltstone and grey mudstone, with many 

coal seams, ironstone nodules or beds and seatearth (palaeosol) 

horizons. The base of the cycle is marked by grey 

mudstones, commonly recognised as nonmarine bands, or 

less commonly as marine bands. Both are important for correlation. 

sandstones are typically very fine- to fine-grained, 

commonly overlain by leached ganisters or unleached gley 

seatearths. The Coal measures accumulated in a delta-top 

environment with large distributary channels, freshwater 

lakes and lagoons with small deltas and crevasse splays, and 

swamps and bogs colonised by plants. laterally widespread 

marine bands (generally lacking diagnostic ammonoids, but 

dominated by foraminifers, Lingula sp., fish remains and a 

shallow marine benthic productid fauna) probably resulted 

from eustatic sea level rises. originally deposited in a broad 

basin, subsequent tectonism has isolated the Coal measures 

into smaller coalfields. 

As defined by stubblefield and Trotter (1957), the base 

of the group is taken at the base of the subcrenatum marine 

Band (sBmB) or at the base of the coal-bearing sequence 

if this marker band cannot be identified. The subcrenatum 

marine Band is absent over much of north Cumbria and has 

a restricted occurrence in west Cumbria. There is also an 

equivalent in north-east england known as the Quarterburn 

marine Band that contains a shallow-marine, benthic, productoid 

fauna (Calver, 1969). 

in north, west and east Cumbria, the solway 

Basin (except the Canonbie area), the stainmore and 

Northumberland troughs, on the Alston Block and in northeast 

Northumberland, the typically repetitive mudstones, 

siltstones, sandstones, thin limestones and thin coals of the 

yoredale Group, lie generally conformably below the base 

of the grey mudstone, siltstone and interbedded pale grey 

sandstone of the pennine lower Coal measures Formation, 

pennine Coal measures Group. in the Canonbie Coalfield, 

the boundary between the stainmore Formation, yoredale 

Group and the pennine lower Coal measures Formation 

is uncertain as to its position and nature (see Jones and 

Holliday, 2006). on the Askrigg Block, and north isle of 

man in the Ballavaarkish (shellag North) Borehole [NX 

4625 0070] the base of the group is also taken at the generally 

conformable base of the pennine lower Coal measures 

Formation. Here, however, dominantly feldspathic sandstones 

of the underlying Rossendale Formation, millstone 

Grit Group are succeeded by the claystone subcrenatum 

marine Band at the base of the Coal measures cyclothemic 

sequence. The base of the warwickshire Group or the 

permo-Triassic unconformity defines the top of the pennine 

Coal measures Group. 

The type area of the pennine Coal measures Group 

is the pennine coalfields, where they are up to 1900 m 

thick near manchester (see waters et al., 2007; waters et 

al.,2009). within the Northern england province they are 

about 1000 m thick in the Canonbie Coalfield where they 

thin westward as they overstep a structural high. They are 

up to 900 m thick in the main area of the Northumberland– 



138 

durham Coalfield, and between 300 and 400 m thick in 

west Cumbria where they thicken offshore to the northwest 

into the solway Basin. on the north isle of man in the 

Ballavaarkish (shellag North) Borehole (see above), about 

16 m of the group was proved. The pennine Coal measures 

Group is westphalian in age, typically langsettian to 

Bolsovian. 

since the pennine Coal measures Group extends into 

onshore southern Great Britain the definitions that follow 

for the constituent formations have been unified with 

those of waters et al. (2009). information relevant solely 

to northern Britain is, however, provided under the subhead 

‘local notes’. 

6.10.1 Pennine Lower Coal Measures Formation 

(PLCM) 

Name 

The formation has historically been referred to as the lower 

Coal measures, as defined by stubblefield and Trotter 

(1957). The name was applied across Britain, despite 

different boundary definitions existing between england 

and scotland (Browne et al., 1999). To distinguish the 

succession present within the pennine Basin from that 

present within the midland valley of scotland and the 

south wales Basin, the formation has been renamed the 

pennine lower Coal measures Formation. 

Lithology 

interbedded grey mudstone, siltstone and pale grey 

sandstone, commonly with mudstones containing marine 

fossils in the lower part, and more numerous and thicker 

coal seams in the upper part. in the lancashire and east 

pennines coalfields the formation can be broadly divided 

into three unnamed members (Chisholm, 1990; Aitkenhead 

et al., 2002). From the base of the subcrenatum marine 

Band to the 80 yard Coal (waters et al., 2009, fig. 13) or 

pasture Coal (waters et al., 2009, fig. 14) the cyclothems 

usually have a marine band at the base and a palaeosol at 

the top, and include micaceous sandstones. Between the 

80 yard or pasture coals and the basin-wide Arley Coal 

(waters et al., 2009, fig. 13) or Kilburn (Better Bed) Coal 

(waters et al., 2009, fig. 14), coal seams are thin and rare, 

only the palaeosol beneath the Kilburn–Arley coals is 

notably leached and marine band faunas are very restricted. 

The sandstones include both micaceous and green, weakly 

micaceous sandstones. Between the Kilburn–Arley coals 

and the base of the vanderbeckei marine Band (waters et 

al., 2009, figs. 13, 14) there is a thick succession of laterally 

impersistent cyclothems that lack true marine bands and 

have thick coals. in the subsurface of the east midlands, 

coal and oil exploration has revealed an abundance of alkali 

basalt lavas and tuffs, limited to the pennine lower Coal 

measures Formation. in the Northumberland and durham 

Coalfield, sheet-like, coarse-grained sandstones, common 

marine bands and thin coals, are present in the pennine 

lower Coal measures. 


The deposits accumulated in a delta-top environment with 

large distributary channels. The main channels, up to 20 

m thick and 20 km wide, were filled by relatively thick, 

sharp-based sandstones (Guion et al., 1995). Between the 

channels were freshwater lakes and lagoons associated with 

deposition of mudstones. The lakes and lagoons were filled 

by small deltas and crevasse splays producing the upwardcoarsening 

siltstones and sandstones. Near-emergent 

surfaces became swamps or raised bogs colonised by plants

which following burial formed coals. subsidence rates 

were low along the southern margin of the pennine Basin 

resulting in relatively few thick seams (waters et al., 1994). 

Northwards, towards the basin depocentre subsidence rates 

are greater and seams split. The cyclothems are typically 

upward-coarsening lake-fills with the principal driving 

force being continuous subsidence. 

some of the cycles, particularly in the early langsettian, 

commence with laterally widespread marine bands that 

probably result from sea level rises (Aitkenhead et al., 

2002). The sandstones present within the lower part of the 

formation are considered to have the same source from 

the north or north-east as the underlying millstone Grit 

(Chisholm et al., 1996). The middle part of the formation 

includes micaceous sandstones sourced from the north, 

and weakly micaceous sandstones sourced from the west 

(Chisholm, 1990; Chisholm et al., 1996; Hallsworth and 

Chisholm, 2000). The latter have the same source as the 

Haslingden Flags of the millstone Grit of yeadonian 

age. The upper part of the formation includes sandstones, 

which appear to be sourced from the west (Hallsworth and 

Chisholm, 2000; Chisholm and Hallsworth, 2005). 

Stratotype 

The type area is the North staffordshire (potteries) Coalfield, 

stoke-on-Trent [sJ 50 90], where there are numerous borehole 

and shaft sections, but few exposures (see waters et al., 2009, 

fig. 13). Reference sections include, for the top boundary: 

mudstone in the vanderbeckei marine Band at miry wood, 

Apedale [sJ 8118 4940], which is to be designated a RiGs 

site (Rees and wilson, 1998). For the top part: from 640 to 

318.5 m in the constructed stratigraphical section (v5 British 

Coal, G7 British Geological survey), Hesketh Back Cut 

(Crosscut), at Chatterley whitfield Colliery, stoke-on-Trent 

[sJ 884 533] (Rees and wilson, 1998). For the lower part 

and base: from surface to 550.7 m depth in the Ridgeway 

Borehole (BGs Registration Number sJ85se/14) [sJ 8923 

5381] (Rees and wilson, 1998). For the base: the River 

little don, langsett [se 2215 0041], which is the basal 

stratotype for the langsettian stage with a section up to 2 m 

thick including the subcrenatum marine Band (owens et al., 

1985); and the Ballavaarkish (shellag North) Borehole [NX 

4625 0070], north isle of man, which includes the pennine 

lower Coal measures Formation from 120.75 m (the top of 

the cored section) to the base of the subcrenatum marine 

Band at about 136.8 m depth (see Chadwick et al., 2001). 


The base of the formation, as defined by stubblefield and 

Trotter (1957), is taken at the base of the dark grey fissile 

mudstone of the subcrenatum marine Band (sBmB) with 

eponymous fossils, or at the base of the lowest coal of the 

coal-bearing sequence if this marker cannot be recognised. 

Typically, the formation rests conformably upon the 

Rossendale Formation (millstone Grit Group) (Figure 8, 

Column 9; Figure 9, Column 17). However, in north, west 

and east Cumbria (Figure 9, Column 13; Figure 14, Column 

1) the solway Basin (Figure 6, Column 7) (except the 

Canonbie area), the stainmore (Figure 9, Column 16) and 

Northumberland troughs (Figure 8, Column 11; Figure 13, 

Columns 3, 4), on the Alston Block (Figure 9, Column 15) 

and in north-east Northumberland (Figure 8, Column 12), the 

formation overlies conformably the repetitive mudstones, 

siltstones, sandstones, thin limestones and thin coals of the 

stainmore Formation (yoredale Group). in the Canonbie 

Coalfield (Figure 8, Column 10), the formation is underlain 

by the stainmore Formation (yoredale Group) though 

the stratigraphical position and nature of the boundary is 

139 

uncertain since the subcrenatum marine Band has not been 

recognised there (see Jones and Holliday, 2006). 

The top of the formation is taken at the base of the 

mudstone of the vanderbeckei marine Band (vdmB) with 

eponymous fossils (Figure 8, Columns 10, 12; Figure 9, 

Columns 13, 16; Figure 10, Column 3; Figure 11, Column 1; 

Figure 13, Columns 3, 4; Figure 14, Columns 1, 2). 

Thickness 

up to 650 m thick in the North staffordshire (potteries) 

Coalfield, and 720 m thick in lancashire. in the Canonbie 

Coalfield the pennine lower Coal measures Formation 

is about 100 m thick (picken, 1988; Jones and Holliday, 

2006). 


Central and northern england, North wales and the north 

isle of man. The formation broadly equates with the 

scottish lower Coal measures and south wales lower 

Coal measures formations, although in the midland valley 

of scotland the definition of the base differs from that of 

the pennine Basin. This reflects the limited recognition of 

the subcrenatum marine Band within the midland valley 

of scotland. 


langsettian. The base of the formation is taken at the base 

of the subcrenatum marine Band (sBmB), which marks the 

base of the langsettian stage. The top is taken at the base of 

the vanderbeckei marine Band (vdmB), which marks the 

base of the duckmantian stage. 

Local notes 

The subcrenatum marine Band, is absent over much of north 

Cumbria and has a restricted occurrence in west Cumbria, 

but has an equivalent in north-east england known as the 

Quarterburn marine Band that contains a shallow marine 

benthic productoid fauna (Calver, 1969). in the north isle 

of man, in the Ballavaarkish (shellag North) Borehole (see 

above), the subcrenatum marine Band contains Lingula 

mytilloides and Gastrioceras subcrenatum. 

6.10.2 Pennine Middle Coal Measures Formation 

(PMCM) 

Name 

The formation has historically been referred to as the 

middle Coal measures, as defined by stubblefield and 

Trotter (1957). The name was applied across Britain, 

despite different boundary definitions existing between 

england and scotland (Browne et al., 1999). To distinguish 

the succession present within the pennine Basin from that 



pennine middle Coal measures Formation. 

Lithology 

interbedded grey mudstone, siltstone, pale grey sandstone 

and commonly coal seams, with a bed of mudstone 

containing marine fossils at the base, and several such 

marine fossil-bearing mudstones in the upper half of the 

unit. in southern Britain the formation can be broadly 

divided into two unnamed members (Aitkenhead et al., 

2002). From the base of the vanderbeckei marine Band to 

the base of the maltby marine Band (waters et al., 2009, 

figs. 13, 14) is similar to the upper member of the lower 

Coal measures. Between the maltby marine Band and 

the top of the Cambriense marine Band marine bands are 



common at the bases of cyclothems and coals are thin. in 

yorkshire, sandstones are generally thicker and coarser than 

is typical of the Coal measures. 


The deposits accumulated in a delta-top environment 

with large distributary channels, similar to that described 

for the pennine lower Coal measures Formation (see 

section 6.10.1). some of the cycles commence with 

laterally widespread marine bands that probably result from 

sea level rises. The lower part of the formation includes 

sandstones with a provenance from the west, representing 

a continuation from the upper part of the pennine lower 

Coal measures (Hallsworth and Chisholm, 2000; Chisholm 

and Hallsworth, 2005). The upper part of the formation 

displays a return to derivation from the north as well 

as the start of a new influx, this time from the east and 

south-east (Hallsworth and Chisholm, 2000; Chisholm and 

Hallsworth, 2005). 

Stratotype 

The type area is the potteries (North staffordshire) 

Coalfield, stoke-on-Trent [sJ 50 90], where there are 

numerous borehole and shaft sections, but few exposures 

(waters et al., 2009, fig. 13). Reference sections include: 

the basal vanderbeckei marine Band at miry wood, 

Apedale [sJ 8118 4940], which is to be designated a 

RiGs site (Rees and wilson, 1998); the upper part of the 

formation, from below the Rowhurst Coal to the top of the 

Cambriense marine Band, from 325.5 to 200.3 m depth, 

in the No. 4 underground borehole (BGs Registration 

Number sJ84Nw/30) [sJ 8392 4850] at Holditch Colliery, 

stoke-on-Trent (Rees and wilson, 1998); the top part of 

the formation, from about 162 m depth at the top of the 

Cambriense marine Band to the bottom of the borehole 

at 183.3 m depth in the No. 1 underground borehole 

(BGs Registration Number sJ85sw/19) [sJ 8396 5029] 

at parkhouse Colliery, stoke-on-Trent (Rees and wilson, 

1998); and the base and lower part of the formation, in 

the Hesketh Back Cut, Chatterley whitfield Colliery from 

318.5 m to the top of the constructed stratigraphical section 

(v5 British Coal, G7 BGs log) [sJ 884 533] (Rees and 

wilson, 1998). The base and lower part also has a reference 

section at duckmanton, north derbyshire [sK 4237 7040], 

which is the basal stratotype section for the duckmantian 

stage, and includes 50 m thickness of pennine middle Coal 

measures above 75 m of pennine lower Coal measures 

(owens et al., 1985). 


The base of the formation, as defined by stubblefield and 

Trotter (1957), is taken at the base of the dark grey, fissile 

mudstone of the vanderbeckei marine Band (vdmB), with 

an eponymous fauna and/or other marine fossils. 

The top of the formation, as defined by stubblefield 

and Trotter (1957), is taken at the top of the dark grey, fissile 

mudstone of the Cambriense marine Band (CAmB), 

with an eponymous fauna and/or other marine fossils. This 

definition is extended to the scottish solway area (Figure 6, 

Column 7; Figure 10, Column 3), which formerly used the 

top of the Aegiranum (skelton) marine Band (AGmB) to 

define the top of the formation. 

Thickness 

up to 600 m thick across the North staffordshire 

Coalfield; about 650 m thick in lancashire; 200 m thick 

in north-west england, and 200–270 m thick around 

Canonbie. 



140 


Central and northern england, North wales. The formation 

broadly equates with the scottish middle Coal measures and 

south wales middle Coal measures formations, although in 

the midland valley of scotland the definition of the top 

differs from that of the pennine Basin. This reflects the 

absence of the Cambriense marine Band within the midland 

valley of scotland. 


duckmantian to Bolsovian. The base of the formation 

is taken at the base of the vanderbeckei marine Band 

(vdmB), which marks the base of the duckmantian stage. 

The top is taken at the base of the Cambriense marine Band 

(CAmB), which occurs within the Bolsovian stage. 

6.10.3 Pennine Upper Coal Measures Formation 

(PUCM) 

Name 

The formation has historically been referred to as the upper 

Coal measures, as defined by stubblefield and Trotter 

(1957). The name was applied across Britain, despite 

different boundary definitions existing between england 

and scotland (Browne et al., 1999). To distinguish the 

succession present within the pennine Basin from that 



pennine upper Coal measures Formation. 

Lithology 

interbedded grey mudstone, siltstone and pale grey 

sandstone, commonly with coal seams, but no mudstones 

containing marine fossils are present. Beds with estheriids 

are common (waters et al., 2009, figs. 13, 14). Coal seams 

are thin. in yorkshire sandstones are common and mainly 

medium-grained. 


The deposits accumulated in a delta-top environment with 

large distributary channels, similar to that described for 

the pennine lower Coal measures Formation (see section 

6.10.1). The sandstones are mainly derived from the 

south-east (Hallsworth and Chisholm, 2000; Chisholm and 

Hallsworth, 2005). The absence of marine bands indicates 

that marine incursions did not extend across the delta top. 

Stratotype 

The type area is the potteries Coalfield, stoke-on-Trent, 

North staffordshire [sJ 50 90], where there are numerous 

borehole and shaft sections, but few exposures (waters 

et al., 2009, fig. 13). Reference sections include: the base 

of the formation, from 5.3 m depth (the start of coring at 

the top of the borehole) to about 162 m depth at the top 

of the Cambriense marine Band in the parkhouse Colliery 

No.1 underground borehole (BGs Registration Number 

sJ85sw/19) [sJ 8396 5029], stoke-on-Trent (Rees and 

wilson, 1998); the base and lower part of the formation, 

from 200.25 m depth to the top of borehole (interpreted 

as the top of the Cambriense marine Band to above the 

Great Row Coal) in the Holditch Quarry No.4 underground 

borehole (BGs Registration Number sJ84Nw/30) [sJ 8392 

4850], stoke-on-Trent (Rees and wilson, 1998); and the 

top and upper part of the formation, from about 317 m to 

faulting beneath the Great Row Coal at about 547 m depth 

in the wolstanton Colliery No.3 shaft (BGs Registration 

Number sJ84Ne/29) [sJ 8606 4800], stoke-on-Trent (Rees 

and wilson, 1998).


The base, as defined by stubblefield and Trotter (1957), 

is taken at the top of the dark grey fissile mudstone with 

marine fossils of the Cambriense marine Band (CAmB). 

in the scottish solway area the base of the upper Coal 

measures was formerly taken at the base of the Aegiranum 

(skelton) marine Band (AGmB) but is now proposed to be 

taken at the top of the Cambriense marine Band to conform 

with the position elsewhere in the pennine Basin. 

The top of the formation is taken at the point in the conformable 

sequence where red or brown mudstones of primary 

origin, typically assigned to the warwickshire Group, 

become predominant over the grey beds, or at the base of 

the sub-permian unconformity. 

Thickness 

The formation is up to 350 m thick in the North staffordshire 

(potteries) Coalfield. picken (1988, fig. 2) suggested a 

general thickness of up to about 650 m in the Canonbie 

Coalfield. 


Central and northern england and North wales. The 

formation broadly equates with the scottish upper 

Coal measures and south wales upper Coal measures 

formations, although in the midland valley of scotland the 

definition of the base differs from that of the pennine Basin. 

This reflects the absence of the Cambriense marine Band 

within the midland valley of scotland. 


Bolsovian to Asturian (westphalian d). The formation is 

characterised by the presence on nonmarine bivalves of the 

Anthraconauta phillipsii and Anthraconauta tenuis zones, of 

late Bolsovian and Asturian (westphalian d) age, respectively. 

Local notes 

in the north-west of the Canonbie Coalfield (Figure 8, 

Column 10) the upper Coal measures, of alluvial 

(‘Barren Measures’) facies, were considered to rest 

unconformably on the middle Coal measures by picken 

(1988), but on the evidence of seismic reflection and 

wireline logging correlation this was not supported by 

Jones and Holliday (2006). The strata are late Bolsovian 

to Asturian (westphalian d) in age and include a Tenuis 

Chronozone fauna with Anthraconaia pruvosti, and Leaia 

bristolensis (see eastwood et al., 1968; lumsden et al., 

1967; Ramsbottom et al., 1978; Jones and Holliday, 2006). 

over much of the west Cumbria Coalfield, strata from the 

upper similis–pulchra Chronozone appear to be cut out 

below the base of the whitehaven sandstone Formation 

(warwickshire Group) (Figure 14, Column 1). 

6.11 WARWICKSHIRE GROUP (WAWK) 

The name ‘warwickshire Group’ (Figure 7), derived from 

the warwickshire Coalfield, was introduced to replace such 

collective terms as ‘Barren (Coal) measures’ and ‘Red 

measures’ that were previously used for predominantly redbed 

strata of alluvial facies (powell et al., 2000; waters et 

al., 2007). in the Central england province the warwickshire 

Group (alluvial (‘Barren Measures’) facies) consists of mainly 

red, brown or purple-grey mudstone, siltstone and sandstone, 

with locally developed pebbly sandstone, conglomerate and 

breccia. The red-beds underwent oxidation at or close to 

the time of deposition. minor components comprise grey 

mudstone, thin coals, lacustrine limestone (‘Spirorbis’ 

141 

limestone) and pedogenic limestone (caliche or calcrete). 

However, the warwickshire Group is also considered to 

extend to the Northern england province (Figure 7) where it 

comprises the eskbank wood, Canonbie Bridge sandstone 

and Becklees sandstone formations at Canonbie (Jones and 

Holliday, 2006; Jones et al., in press), and the stand-alone 

fluvial and fluviolacustrine whitehaven sandstone Formation 

in north and west Cumbria (Akhurst et al., 1997). 

The base of the group in the Canonbie Coalfield is taken 

at the conformable and gradational base of the eskbank 

wood Formation where the first major red-bed strata 

overlie the grey mudstone-dominated pennine upper Coal 

measures Formation. The sharp, unconformable base of the 

permian (variscan) unconformity, overlying the Becklees 

sandstone Formation, defines its top. The base of the 

group in north and west Cumbria is taken at the base of the 

whitehaven sandstone Formation where the non-reddened, 

cyclical, mudstone-dominated succession with thin coals of 

the underlying uppermost pennine Coal measures Group 

are succeeded unconformably by red sandstones. over 

much of the west Cumbria Coalfield, strata from the upper 

similis–pulchra Chronozone appear to be cut out below the 

base of the whitehaven sandstone Formation. The base of 

the permian unconformity defines the top of the group (see 

Akhurst et al., 1997). 

The Type area of the warwickshire Group is the 

warwickshire Coalfield in central england, where the 

duckmantian to early permian (Autunian) succession 

attains its fullest thickness of 1225 m (see powell et al., 

2000; waters et al., 2007; waters et al., 2009). in the 

Canonbie Coalfield the group may be up to perhaps 500 m 

thick, whilst in north and west Cumbria it is at least 300 m 

thick. in both areas the group is late Bolsovian to Asturian 

(westphalian d) in age. 

6.11.1 Eskbank Wood Formation 

Name 

Newly named. The formation is exposed along the River 

esk, Canonbie area, opposite eskbank wood. see Jones and 

Holliday (2006); Jones et al. (in press). 

Lithology 

interbedded red mudstone (claystones and siltstones), 

fine- to medium-grained sandstones, calcrete palaeosols, 

thin beds of ‘Spirorbis’ limestone and Estheria-bearing 

mudstones. sparse thin coals and grey mudstones are 

present in the lower part of the formation; some of these 

coals have been oxidised and altered to limestone (Jones 

and Holliday, 2006; Jones et al., in press; see also mykura, 

1960). mudstones form 60–70 per cent of the formation, 

with sandstones forming most of the rest. 


deposition on an alluvial plain with lakes. The flood plain 

alternating from poorly to well drained. 

Stratotype 

The type area is Hush pool, River esk [Ny 39149 77055 

to 39194 76953]. Approximately 75 m of nearly continuous 

outcrops of the formation are present along the eastern 

bank of the River esk. Reference sections include the Forge 

diamond Bore (BGs Registration Number Ny37Ne/7) 

[Ny 39456 76720] from 72.8 to 235.5 m depth (the full 

thickness being cored), and the Becklees Borehole (BGs 

Registration Number Ny37se/3) [Ny 35166 71578] from 

653 to 816.8 m depth (the formation being cored from 

744.41 m depth to its base). 




The base of the formation was not identified at outcrop and 

is defined in boreholes. The boundary is taken at the first 

major red-bed strata overlying the grey mudstone-dominated 

pennine upper Coal measures Formation (Figure 8, Column 

10). it is a conformable, gradational boundary. in the 

Becklees Borehole (see above) the base of the formation (at 

816.8 m depth) is defined by the last significant downhole 

occurrence of primary red-bed lithologies. in this instance 

it comprises 1.3 m of mottled reddish brown and greenish 

grey silty mudstone with abundant carbonate nodules. These 

nodules are interpreted as pedogenic calcrete glaebules 

and represent the first good evidence for the development 

of primary red-bed conditions. A limited number of red 

lithologies are known below 816.8 m depth, but it is not 

known whether these represent primary red-beds or could be 

linked to a later secondary reddening event. The gradational 

boundary to the formation is well demonstrated by the 

reversion higher in the borehole to grey lithologies. This 

includes a prominent coal (the ‘High’ Coal), which is about 

1 m in thickness and must represent a significant amount of 

time in which reducing conditions prevailed. in the Forge 

diamond Bore (see above) the base is taken at the change 

from pale greenish mudstones to red and green mudstones 

at 235.5 m depth. The lower boundary is difficult to pick in 

uncored boreholes, but analysis of cored boreholes shows 

that close to the base of the formation the distinctive ‘High’ 

Coal is typically present, and can be identified from suitable 

geophysical logs (e.g. sonic, density). it is suggested that the 

position of this coal be taken as the base of the formation 

where core data are absent. 

The top of the formation is taken at the base of the lowermost 

sandstone bed of the Canonbie Bridge sandstone 

Formation (Figure 8, Column 10). This is typically a thick 

(20–30 m) multistorey sandstone complex. The abrupt 

junction can be examined at outcrop at [Ny 39194 76953] 

and has also been proven in numerous boreholes, including 

the Becklees Borehole (see above) (cored depth: 653 m; 

geophysical log depth: 656 m), and those at Broadmeadows 

(BGs Registration Number Ny37Ne/15) [Ny 37646 

76265] (geophysical log depth: 176.6 m) and Glenzierfoot 


(geophysical log depth: 368.2 m). 

Thickness 

in the Forge diamond, Becklees and Glenzierfoot boreholes 

(see above) the formation is about 163 m, 164 m and 146 

m thick respectively. in the Rowanburnfoot Bore (BGs 

Registration Number Ny47Nw/27) [Ny 41031 75743] it 

is 175 m thick. 


The formation is restricted to part of the Canonbie Coalfield 

between the evertown [Ny 3639 7594] and the Rowanburn 

[Ny 41140 7687] areas. it is also known in its subsurface 

south-western extension, where it has been proven for at 

least a distance of approximately 6 km. 


late Bolsovian (westphalian C) to Asturian (westphalian 

d). The section along the eastern bank of the River esk north 

of Canonbie Bridge comprises some mudstones that contain 

a nonmarine fauna, particularly bivalves, at various points 

in the section. These have been identified as Anthraconauta 

phillipsii, A. aff. phillipsii, A. cf. tenuis, A. cf. wrightii, possibly 

Anthracomya pruvosti and also ostracods (A. e. Trueman in 

Barrett and Richey 1945, p. 39). Trueman suggested that this 

indicates the A. tenuis or even the A. prolifera Nonmarine 



142 

Bivalve Zone of Trueman and weir (1946), which are 

indicative of an Asturian (westphalian d) age. 

6.11.2 Canonbie Bridge Sandstone Formation 

Name 

Newly named. outcrops of this formation occur in the River 

esk upstream and downstream of Canonbie Bridge. see 

Jones and Holliday (2006); Jones et al. (in press). 

Lithology 

interbedded fine- to coarse-grained reddish brown to 

greenish grey, moderately- to poorly sorted sandstones 

(50–70 per cent) and reddish brown mudstones and 

reddish brown, well-drained palaeosols including calcretes. 

sandstones can be micaceous and are typically thick (10–30 

m) forming sharp to erosively based channel sandstones 

in multistorey successions, cross-bedded and some show 

upwards-fining. intraformational mudstone conglomerates 

occur scattered throughout the sandstones but are more 

common at channel bases. in hand specimen the sandstones 

contain a noticeable component of greenish grey grains, 

which, in thin section, can be seen to be lithic clasts. This 

high lithic component gives the sandstones a characteristic 

gamma ray log signature, with GR values ranging from 

56–120 Api (mean 97.3, median 99.53 Api). 


deposition generally on a well-drained alluvial plain with 

large fluvial systems and rare ephemeral floodplain lakes. 

sporadic periods of poorer drainage. 

Stratotype 

The formation outcrops at its type locality along the River 

esk for 250 m south of Canonbie Bridge, for example at 

[Ny 39551 76501], and in discontinuous exposures for 

about 600 m to the north of the bridge, for example at [Ny 

39502 76735] and [Ny 39317 76792]. A reference section 

is the Forge diamond Bore (BGs Registration Number 

Ny37Ne/7) [Ny 39456 76720], which cored the lower part 

of the formation from about 2.2 to 72.8 m depth. 


The base of the formation is taken at the base of the 

lowermost sandstone bed in a 20–30 m thick multistorey 

sandstone complex resting on the interbedded mainly 

mudstone and sandstone of the eskbank wood Formation 

(Figure 8, Column 10). The abrupt junction can be examined 

at outcrop at [Ny 39194 76953] and has also been 

proven in numerous boreholes, including those at Becklees 


(cored depth: 653 m; geophysical log depth: 656 m), 

Broadmeadows (BGs Registration Number Ny37Ne/15) 

[Ny 37646 76265] (geophysical log depth: 176.6 m), and 

Glenzierfoot (BGs Registration Number Ny37se/2) [Ny 

36514 74275] (geophysical log depth: 368.2 m). in the 

Forge diamond Bore (see above) the base is taken at a 0.6 

m-thick conglomerate bed at 72.8 m depth. 

At outcrop [Ny 39360 76310] and [Ny 39812 75760] the 

upper boundary is taken at the abrupt junction between the 

fine- to coarse-grained reddish brown lithic sandstones of 

the Canonbie Bridge sandstone Formation and the overlying 

softer, orange brown, fine- to medium-grained sandstones 

that lack appreciable lithic grains (Becklees sandstone 

Formation) (Figure 8, Column 10). in uncored boreholes the 

boundary is marked by a shift in the gamma ray log to lower 

values, reflecting the change in sandstone composition from 

lithic rich (higher GR values) to lithic poor, ‘cleaner’ sand-

stones with lower GR values. This can be seen for example 

at 485.3 m and 214 m depth in the Becklees and Glenzierfoot 

boreholes (see above) respectively. 

Thickness 

The formation varies in thickness. it is 131 m and 154 m 

thick in the Broadmeadows and Glenzierfoot boreholes (see 

above) respectively. it has a maximum thickness of 168 m 

in the Becklees Borehole (see above). 


The formation is restricted to part of the Canonbie Coalfield 

between the evertown [Ny 3639 7594] and Rowanburn 

[Ny 41140 7687] areas. it is also known in its subsurface 

south-western extension, where it has been proven for at 

least a distance of approximately 6 km. 

Age 

Asturian (westphalian d). 

6.11.3 Becklees Sandstone Formation 

Name 

The new name is derived from the Becklees Borehole 

(BGs Registration Number Ny37se/3) [Ny 35166 71578], 

which proves the greatest thickest of this formation. see 

Jones and Holliday (2006); Jones et al. (in press). 

Lithology 

interbedded red sandstones (70–90 per cent) and reddish 

brown mudstones and reddish brown palaeosols including 

calcretes. sandstones are fine- to medium-grained, orange 

brown to bright reddish brown and pinkish brown, moderately 

to well sorted and typically lack mica. sandstones are 

generally cross-bedded and occur in thick successions 

(10–30 m thick), forming sharp to erosively based channel 

sandstones in multistorey units, some showing upwardsfining. 

in hand specimen the sandstones contain noticeably 

fewer lithic clasts than the underlying Canonbie Bridge 

sandstone Formation; this is confirmed by thin section 

analysis. The sandstones have lower gamma ray Api values 

compared to the underlying Canonbie Bridge sandstone 

Formation, with GR values ranging from 39–120 Api 

(mean 77.1, median 74.02 Api). limestones and thin coals 

are indicated in cuttings descriptions from the Becklees 

Borehole (see above), although these do not appear to be 

common and were not recorded at outcrop. 


deposition on a well-drained alluvial plain with large 

fluvial systems and rare ephemeral floodplain lakes. 

Stratotype 

The formation outcrops at its type locality along the River 

esk, Canonbie area, opposite dead Neuk [Ny 39360 

76310], where approximately 28 m are present, including 

the base. Reference sections include outcrops along the 

River esk at mason’s stream [Ny 39813 75760]. 


The base of the formation occurs at outcrop at [Ny 39360 

76310] and [Ny 39812 75760]. it is taken at the abrupt 

junction where fine- to coarse-grained reddish brown lithic 

sandstones of the Canonbie Bridge sandstone Formation 

are overlain by softer, orange brown, fine- to mediumgrained 

sandstones that lack appreciable lithic grains of 

the Becklees sandstone Formation (Figure 8, Column 10). 

in uncored boreholes the boundary is marked by a shift 

143 

in the gamma ray log to lower values, reflecting the 

change in composition from lithic rich (higher GR values) 

sandstones of the Canonbie Bridge sandstone Formation 

to lithic poor, ‘cleaner’ sandstones with lower GR values 

(Becklees sandstone Formation). This can be seen for 

example at 485.3 m depth in the Becklees Borehole (see 

above) and 214 m depth in the Glenzierfoot Borehole (BGs 

Registration Number Ny37se/2) [Ny 36514 74275]. 

unusual polygonal cracks have been recorded at the base 

of the formation along the River esk at [Ny 39360 76310]. 

The top of the formation is taken at the sharp boundary 

beneath permian rocks (Figure 8, Column 10). This marks 

the variscan unconformity. 

Thickness 

The full thickness of the formation is not proven but ranges 

from zero to a maximum of 203.6 m in the Becklees 

Borehole (see above). 

Distribution 

The formation is restricted to the central parts of the 

Canonbie syncline, between the evertown Borehole (BGs 

Registration Number Ny37Ne/14) [Ny 36390 75938], 

the Becklees Borehole (see above), and the Knottyholm 


39501 77124]. 

Age 

Asturian (westphalian d). 

6.11.4 Whitehaven Sandstone Formation (WS) 

Name 

The name is derived from the area around whitehaven in 

west Cumbria. 

Lithology 

A red-bed succession. The lower part, the Bransty Cliff 

sandstone member (the whitehaven sandstone of Akhurst 

et al., 1997), comprises red to deep purple or purplish 

brown, cross-bedded, micaceous, medium- to coarse-grained 

sandstone. There are interbeds of pink to red or grey mudstone 

and siltstone and thin palaeosols are present locally. These 

beds are overlain by a thick heterogenous, dominantly red 

succession (the millyeat member) of mudstone, sandstone 

and marl with thin coals and limestones with Spirorbis sp. 


The lower part of the formation was deposited from a 

major braided river system that flowed from the north-east. 

The upper part of the formation represents deposition in 

interdistributary bay or lacustrine environments with minor 

river channels (Akhurst et al., 1997). The reddening was 

either primary or early diagenetic. 

Stratotype 

partial type sections in the formation include the whitehaven 

Harbour cliff sections around [NX 974 192] where the 

lower arenaceous part of the formation (the Bransty Cliff 

sandstone member with mainly sandstone and subsidiary 

mudstone and siltstone interbeds) is well exposed, and 

the Frizington Hall Borehole (BGs Registration Number 

Ny01Nw/174) [Ny 0189 1710] from 12.8 m depth to the 

bottom of the borehole at 174.65 m depth. 


The base of the formation is taken where the non-reddened, 

cyclical, mudstone-dominated succession with thin coals 



of the underlying pennine Coal measures Group are 

succeeded unconformably by red sandstones (Figure 9, 

Column 13; Figure 14, Column 1). The unconformity cuts 

down to the Aegiranum marine Band (AGmB) or, locally 

older strata (Akhurst et al., 1997). 

The upper boundary of the formation is the base of the 

sub-permian unconformity, which is overlain by the coarse, 

poorly bedded, poorly to moderately sorted, generally massive, 

matrix or clast-supported, typically pebble-grade, breccias 

of the permian Brockram (Appleby Group). 

Thickness 

The formation is at least 280 m thick. The Bransty Cliff 

sandstone member is at least 100 m thick. The millyeat 

member is 180 m thick. 


within the Northern england province the formation is 

recognised in north and west Cumbria. 


late Bolsovian to early Asturian (westphalian d) as indicated 

by plant remains and the presence of the nonmarine bivalve 

Anthraconauta phillipsii (eastwood et al., 1931). To the 

north-east similar strata have an Asturian (westphalian d), 

Tenuis Chronozone fauna (eastwood et al., 1968). 


see also Appendix 1. members of the whitehaven sandstone 

Formation, in ascending stratigraphical order, include: 

6.11.4.1 BransTy CliFF sanDsTone MeMBer (ByCs) 

Name 

previously named the whitehaven sandstone by eastwood 

et al. (1931; see also Akhurst et al., 1997; Brockbank, 1891; 

Jones, 1993). 

Lithology 

Red, to deep purple or purplish brown, cross-bedded, 

micaceous, medium- to coarse-grained sandstone, with 

subsidiary mudstone and siltstone interbeds, and thin 

palaeosols. 


The unit was deposited from a major braided river system 

that flowed from the north-east. The reddening was either 

primary or early diagenetic. 

Stratotype 

The type section is the whitehaven harbour cliffs [NX 

9735 1950 to 9750 1895] where the mainly sandstone and 

subsidiary mudstone and siltstone interbeds of the member 

are well exposed. 


The lower boundary, at the base of the lowest major reddened 

channel sandstone unit, is unconformable cutting down 

to the interbedded mudstones, siltstones, and sandstones, 

with coal seams, of the pennine middle Coal measures 




144 

The upper boundary with the mudstone dominated 

millyeat member, is at the top of the highest major 

channel sandstone unit in the Bransty Cliff sandstone 

member. 

Thickness 

Greater than 100 m 


The west Cumbria Coalfield. 

Age 

Bolsovian (westphalian C) to Asturian (westphalian d). 

6.11.4.2 MillyeaT MeMBer (MyTB) 

Name 

see Akhurst et al. (1997); also Brockbank (1891); 

eastwood et al. (1931); Jones (1993). in the former name 

‘millyeat Beds member’ the term ‘Beds’ has now been 

abandoned. 

Lithology 

A thick heterogeneous, dominantly red succession of 

purple–red mudstone, with subsidiary sandstone and 

siltstone, and minor ‘marl’, thin coals and thin beds of 

limestone with Spirobis sp. 


The member was deposited in interdistributary bay or 

lacustrine environments with minor river channels (Akhurst 

et al., 1997). The reddening was either primary or early 

diagenetic. 

Stratotype 

The type section is the Frizington Hall Borehole (BGs 

Registration Number Ny01Nw/174) [Ny 0189 1710] from 

12.8 to 155 m depth. A reference section is the millyeat 

Borehole (BGs Registration Number Ny01Nw/175) [Ny 

023 178] from about 7.5 to 158 m depth. 


The base of the unit is the top of the highest major channel 

sandstone unit in the Bransty Cliff sandstone member 


The upper boundary of the member is the sub-permian 

unconformity, which is overlain by the coarse, poorly bedded, 

poorly to moderately sorted, generally massive, matrix 

or clast-supported, typically pebble-grade, breccias of the 

permian Brockram (Appleby Group). 

Thickness 

up to 180 m maximum. 


west Cumbria Coalfield. 

Age 

Bolsovian (westphalian C) to Asturian (westphalian d).

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64–68. 



Appendix 1 Alphabetical listing of lithostratigraphical units 

Alphabetical listing of lithostratigraphical units (by group) 

and their BGs lexicon of Named Rock units computer 

codes (where allocated). 



154 

definitive information about all the lithostratigraphical 

units listed below can be found in the BGs lexicon of 

Named Rock units, accessible on the BGs website at http:// 

www.bgs.ac.uk/lexicon (see also Appendices 2 and 3). 

Supergroup Group Formation 

Bathgate Hills volcanic (BHv) 

Member 

Bathgate (BATH) Kinghorn volcanic (KNv) 

salsburgh volcanic (sAlv) 

Gillfoot sandstone (Gisd) 

Fell sandstone (Fell) 

powillimount sandstone (posd) 

Rascarrel (RAsC) 

Bewcastle (BwCB) 

Border (BdR) 

Cambeck (CmBB) 

lyne (lyNe) 

easton Anhydrite 

lynebank (lyN) 

main Algal (mAN) 

No relationship 

enterkin mudstone (eNT) 

southerness limestone (solm) 

limestone Coal (lsC) 

Black metals (BKme) 

Kilbirnie mudstone (Klmd) 

Clackmannan (CKN) 

lower limestone (llGs) 

Ayrshire Bauxitic Clay (ABC) 

passage (pGp) 

upper limestone (ulGs) 

Townburn sandstone (TwN) 

Troon volcanic (Tvl) 

Craven (CRAv) 

Bowland shale (BsG) 

Hodderense limestone (BoH) 

Ashfell limestone (AFl) 

scarlett point (sCpT) 

scarlett volcanic (sCv) 

Carboniferous 

limestone (Cl) 

Great scar limestone 

(GsCl) 

Ashfell sandstone (AFs) 

Balladoole (Bool) 

Breakyneck scar limestone (BRe) 

Brownber (BNBF) 

Chapel House limestone (CHpl) 

Coldbeck limestone (ClK) 

Cracoe limestone (CCoe) 

dalton (dlB) 

danny Bridge limestone (dBl) 

derbyhaven (dBH) 

eskett limestone (esKT) 

Fawes wood limestone (Fwl) 

sandwick (isle of man) (swiK) 

skillicore (sKil) 

Turkeyland (TuRK)

Supergroup Group Formation 

Frizington limestone (FRli) 

Garsdale limestone (GAl) 

Member 

Kilnsey (Klsl) 

Knipe scar limestone (KNl) 

Knockrushen (KNRN) 

scaleber Force limestone (sFlm) 

scaleber Quarry limestone (sQlm) 

malham (mAlm) 

Cove limestone (Cvls) 

Gordale limestone (Gdll) 

Carboniferous 

limestone (Cl) 

martin limestone (mTl) 

melmerby scar limestone (mel) 

park limestone (pKl) 

potts Beck limestone (pBK) 

Red Hill limestone (RHo) 

scandal Beck limestone (sCBl) 

Tom Croft limestone (TCl) 

urswick limestone (ul) 

Coupland syke limestone (Cosl) 

park Hill limestone (pAl) 

drumwhirn (dRwN) 

Kirkbean Cementstone (KiCm) 

Ballagan (BGN) 

Birrenswark volcanic (BiRv) 

Cottonshope volcanic (Covo) 

lindsayston Burn (lsBu) 

orroland (oRR) 

wall Hill (wlH) 

Ascog (Aso) 

Broadlee Glen sandstone (BRlG) 

eileans sandstone (elN) 

inverclyde (iNv) 

Gourock sandstone (GKA) 

Clyde sandstone (Cyd) 

Knocknairshill (KKs) 

laggantuin Cornstone (lGT) 

millport Cornstones (mlC) 

millstone point sandstone (mps) 


Kelso volcanic (KT) 

overtoun sandstone (ovs) 

doughend sandstone (dHs) 

Kinnesswood (KNw) 

Roddam dene Conglomerate (RdCo) 

Hebden (HeBd) 

marsden (mARsd) 

Foulport mudstone (FmN) 

west Bay Cornstone (wBC) 

millstone Grit (mG) 

pendleton (peNdl) 

Rossendale (Rosse) 

samlesbury (sAml) 

silsden (sils) 

langness Conglomerate (lNCo) 

penny Farm Gill (pFd) 

pendle Grit 

Ravenstonedale (Rvs) pinskey Gill (pNKG) 

Raydale dolostone (Rdo) 

shap village limestone (sHvi) 

155 



Supergroup Group Formation Member 

No relationship Ravenstonedale (Rvs) 

Coal measures 



pennine Coal measures 

(pCm) 

scottish Coal measures 

(CmsC) 

No relationship strathclyde (syG) 

stone Gill limestone (sTe) 

Cockermouth volcanic (CKml) 

marsett (mAsA) duddon Conglomerate (duCo) 

pennine lower Coal measures (plCm) 

pennine middle Coal measures (pmCm) 

pennine upper Coal measures (puCm) 

scottish lower Coal measures (lCms) 

scottish middle Coal measures (mCms) 

scottish upper Coal measures (uCms) 

Aberlady (ABy) 

Anstruther (ARBs) 

Charles Hill volcanic (CHvo) 

Arthur’s seat volcanic (Asv) 

Birgidale (Bid) 

Clyde plateau volcanic (Cpv) 

156 

Auchineden lava 

Baston Burn lava 

Beith lava 

Black mount lava 

Boyd’s Burn lava 

Burncrooks volcaniclastic 

Burnhouse lava 

Campsie lava 

Carbeth lava 

Carron Bridge lava 

Cochno lava 

Corrie lava 

Craigdouffie lava 

Craigentimpin lava 

Cringate volcaniclastic 

darvel lava 

denny muir lava 

drumnessie lava 

dumdruff Hill lava (dHlA) 

eaglesham lava 

Faughlin lava 

Fereneze lava 

Fin Glen lava 

Fintry Hills lava 

Gargunnock Hills lava 

Garvald lava 

Glenburn volcaniclastic (GBv) 

Gleniffer lava 

Gowk stane volcaniclastic (GowK) 

Greenan Castle pyroclastic (GCp)


No relationship strathclyde (syG) 

Clyde plateau volcanic (Cpv) 

Fife Ness (FNB) 

Garleton Hills volcanic (GHv) 

Gullane (Gul) 

Kirkwood (KRw) 

laggan Cottage mudstone (lNT) 

157 

Greenside volcaniclastic 

Greeto lava 

Harelaw lava 

Holehead lava 

Kilbarchan lava 

Kilsyth Hills lava 

Knowehead lava 

laird’s Hill lava 

laird’s loup lava 

langhill lava 

largs lava 

lees Hill lava 

loup of Fintry lava 

lower Flow moss lava 

lower lecket Hill lava 

marshall moor lava 

misty law Trachytic 

moyne moor lava (mmlA) 

mugdock lava 

Neilston lava (NNlA) 

Noddsdale volcaniclastic 

North Campsie pyroclastic 

overton lava 

sargeantlaw lava 

saughen Braes lava 

shelloch Burn lava 

skiddaw lava 

slackdown lava 

slackgun volcaniclastic 

spout of Ballochleam lava 

strathgryfe lava 

stronend volcaniclastic 

Tambowie lava 

Tappetknowe lava 

Touch House lava 

upper Flow moss lava 

upper lecket Hill lava 

Bangley Trachytic (ByTRC) 

east linton lava (ellA) 

Hailes lava (HslA) 

North Berwick pyroclastic (NBpy) 







lawmuir (lwm) 

pathhead (pdB) 

pittenweem (pmB) 

sandy Craig (sCB) 

west lothian oil-shale (wlo) 

No relationship stockdale Farm (sTFA) 

Becklees sandstone 

Canonbie Bridge sandstone 

warwickshire (wAwK) eskbank wood 

yoredale (yoRe) 

whitehaven sandstone (ws) 

Alston (AG) 

Closeburn limestone (Clo) 

stainmore (smGp) 

Tyne limestone (Tyls) 

158 

Craigmaddie muir sandstone (CRms) 

douglas muir Quartz-Conglomerate 

(dmQ) 

Calders (Cde) 

Hopetoun (HoN) 

Bransty Cliff sandstone (ByCs) 

millyeat (myTB) 

Askham limestone (AsKl) 

eelwell limestone (ewl) 

Five yard limestone (Fyl) 

Four Fathom limestone (FFl) 

Great limestone (Gl) 

Jew limestone (Jwl) 

oxford limestone (oXl) 

scar limestone (sCl) 

Three yard limestone (Tyl) 

Tynebottom limestone (TBl) 

Arbigland limestone (ARlm) 

dun limestone (dNl) 

wintertarn sandstone (wTRs)

Appendix 2 BGs lexicon of Named Rock units computer codes 

BGs lexicon of Named Rock units computer codes and 

lithostratigraphical beds shown in Figures 6 and 8, and 

any lower palaeozoic lithostratigraphical units referred to. 

Lexicon code Bed (unless otherwise stated) 

AGMB Aegiranum mB 

AKB Archerbeck Beds 

AMMB Amaliae mB 

AOB Archerbeck ochre Bed 

APL Appletree lst 

ASKL Askham lst 

BARL Barrasford lst 

BGSL Bogside lst 

BHGL Brainshaugh lst 

BMET Black metals mB 

BNKL Bankhouses limestones 

BPLS Blae pot lst 

BRDL Bridge lst 

BSDL Belsay dene lst 

BTL Barrock Top lst 

BUBE Burns Beds 

BULS Burdiehouse lst 

BZB Bryozoa Band 

CALS Callant lst 

CAMB Cambriense mB 

CAS Castlecary lst 

CBLM Cawledge Bend lst 

CEBS Carlyle Beds 

CFL Common Flat lst 

CGLM Crag lst 

CHMB Cockhill mB 

CHML Carham lst 

CMB Colsterdale marine Beds 

CORL Corbridge lst 

CROL Crow lst 

CSL Cockleshell lst 

CTB Clattering Band 

CUL Cushat lst 

CWELL Colwell lst 

CWMB Clown mB 

DDL duddo lst 

DIB dinwoodie Beds 

DNL dun lst 

DNML denton mill lst 

DPL dunkpool lst 

DSL desoglin lst 

DTNL dalton lst 

E1A1 Cravenoceras leion mB 

E2A1 Cravenoceras cowlingense mB 

159 

Key: Fm - Formation; l = lower; lst = limestone; m = middle; 

mB = marine Band; sst = sandstone; u = upper. 

EMMB edmondia mB 

ESL ellery syke lst 

FENL Fenwick lst 

FLL Fourlaws lst 

G1A1 Cancelloceras cancellatum mB 

G1B1 Cancelloceras cumbriense mB 

GGL Greengate well lst 

GNWL Greenhow lst 

GUMB Gubeon mB 

GV Glencartholm volcanic Beds 

GVB Girvanella Nodular Band 

GYL Gayle lst 

H1B1 Homoceras beyrichianum mB 

HAMB Harvey mB 

HGEL Hargate end lst 

HGLS Hogg lst 

HLAB Hillend Algal Band 

HMMB High main mB 

HNB Harden Beds 

HNMB Honley mB 

HSCL Hardraw scar lst 

HTMB Haughton mB 

HUR Hurlet lst 

HWL Hawes lst 

HYMB Hylton mB 

ILS index lst 

IPL iron post mB 

ISMB Isohomoceras subglobosum mB 

KBL Kingbridge lst 

KHB Kershopefoot basalts 

KLMB Kays lea mB 

KMB Kirkby’s mB 

KMMB Knottyholm mB 

KTLS Kinmont lst 

LANL lanercost lst 

LAQB l Antiquatonia Band 

LARS larriston sst Beds 

LBWL l Bath-house wood lst 

LCRT low Carriteth lst 

LDML l demesne lst 

LFTL l Felltop lst; 

LGFLL l Gunnerton Fell lst 

LGLL lad Gill lst 

LGMB langley mB 

LHL leahill lst 



LKL lickar lst 

LLLM l little lst 

LM1 First lst 

LM2 second lst 

LM3 Third lst 

LM4 Fourth lst 

LM5 Fifth lst 

LM6 sixth lst 

LM7 seventh lst 

LMIL l millerhill lst 

LNN lonan Formation (ordovician) 

LOCH l Camphill lst 

LOL l oakwood lst 

LOMB lowstone mB 

LSMB listeri mB 

LSRL little strickland lst 

LSTL l stonesdale lst 

LTL low Tipalt lst 

LTLS little lst 

LTMB little mB 

LWSL lawston lst 

MANX manx Group (ordovician) 

MDL middle lst 

MFC mell Fell Conglomerate (devonian) 

MIL millerhill lst 

MKFG mirk Fell Ganister 

MKFI mirk Fell ironstone 

MTMB maltby mB 

NL Naworth lst 

NWBB Naworth Bryozoa Band 

NWL Newton lst 

NWNL Netherwitton lst 

OKL oakwood lst 

OKSS oakshaw sst 

ORS old Red sst supergroup (devonian) 

PCL piper’s Cross lst 

PFLS penchford lst 

PGL peghorn lst 

PHL pike Hill lst 

PILS pigdon lst 

PLDL plashetts dun lst 

PNLS penton lst 

QBMB Quarterburn mB 

QMB Queenslie mB 

RBLL Redhouse Burn l lst 

RBML Redhouse Burn m lst 

RBUL Redhouse Burn u lst 

RDL Redesdale lst 

RGL Raughton Gill lst 

RLM Rough lst 

RNL Robinson lst 

RSMB Riddings mB 

RTMB Rowanburnfoot mB 

RWNL Rawney lst 

RYMB Ryhope mB 

SBMB subcrenatum mB 

SCMB st Andrew’s Castle mB 



160 

SCOT scott Beds 

SCSL stump Cross lst 

‘SDV’ ‘st davids volcanic Beds’ 

SFMB shafton mB 

SHL spy Hole lst 

SHMB sandwich mB 

SHWC shap wells Conglomerate Fm (devonian) 

SIL simonstone lst 

SNMB skelton mB 

SOMB sutton mB 

SPL single post lst 

STFL styford lst 

SUS sugar sands lst 

SWMB stobbswood mB 

SWOL shotto wood lst 

SWYMB solway mB 

SXYL six yard lst 

SYGL Syringothyris lst 

THL Thornborough lst 

THSD Thirlstane Beds 

TMB Tait’s mB 

TMBL Tombstone lst 

TOHO Top Hosie lst 

UAQB u Antiquatonia Band 

UBWL u Bath-house wood lst 

UDML u demesne lst 

UFTL u Fell Top lst 

UGFL u Gunnerton Fell lst 

UMIL u millerhill lst 

UOL u oakwood lst 

USTL u stonesdale lst 

VDMB vanderbeckei mB 

VMB viaduct mB 

WBB whitberry Band 

WBMB west Braes mB 

WDEL woodend lst 

WTL white lst 

WTLL watchlaw lst

Appendix 3 Alphabetical listing of obsolete lithostratigraphical 

terms 

Alphabetical listing of obsolete lithostratigraphical terms 

mentioned in the text, and the units they are now equivalent 

to or included within. 

161 

For BGs lexicon of Named Rock units computer codes see 

Appendix 1. 

Obsolete term: Now equivalent to or included within: 

Acre limestone Three yard limestone member, Alston Formation 

Alston Group yoredale Group 

Arbigland limestone Formation Arbigland limestone member, Tyne limestone Formation 

Auchineden lavas Auchineden lava member, Clyde plateau volcanic Formation 

Ayrshire Bauxitic Clay Formation Ayrshire Bauxitic Clay member, passage Formation 

Bangley member Bangley Trachytic member, Garleton Hills volcanic Formation 

Barren (Coal) measures warwickshire Group 

Basal Cementstones Kirkbean Cementstone member, Ballagan Formation 

Basal Group slackdown member, Clyde plateau volcanic Formation 

‘Basal sandstone’ drumwhirn member, Ballagan Formation 

Baston Burn Group Baston Burn lava member, Clyde plateau volcanic Formation 

Bathgate lavas Bathgate Hills volcanic Formation 

‘bedded agglomerate of Greenan Castle’ Greenan Castle pyroclastic member, Clyde plateau volcanic 

Formation 

Beith lavas Beith lava member, Clyde plateau volcanic Formation 

Bewcastle Beds Bewcastle member, lyne Formation 

Beyrichoceras hodderense Bed Hodderense limestone Formation 

Birdoswald limestone Group Tyne limestone Formation, yoredale Group 

Black metals Black metals member, limestone Coal Formation 

Black mount Group Black mount lava member, Clyde plateau volcanic Formation 

Blea Tarn limestones Breakyneck scar limestone Formation 

Bowland shale Group Bowland shale Formation 

Boyd’s Burn lavas Boyd’s Burn lava member, Clyde plateau volcanic Formation 

Broadlee Glen sandstones Formation Broadlee Glen sandstone member, Clyde plateau volcanic 

Formation 

Bucchleuch limestone Four Fathom limestone member, Alston Formation 

Burncrooks pyroclastic member Burncrooks volcaniclastic member, Clyde plateau volcanic 

Formation 

Burnhouse lavas Burnhouse lava member, Clyde plateau volcanic Formation 

Burntisland lavas Kinghorn volcanic Formation, Bathgate Formation 

Carbeth lavas Carbeth lava member, Clyde plateau volcanic Formation 

Carboniferous limestone Carboniferous limestone supergroup 

Carboniferous limestone series Clackmannan Group 

Carron Bridge lavas Carron Bridge lava member, Clyde plateau volcanic Formation 

Catsbit limestone Great limestone member 

Charles Hill volcanic Beds Charles Hill volcanic member, Anstruther Formation 

Chief limestone Group Great scar limestone Group and Alston Formation (yoredale 

Group) 



Coal measures Group pennine Coal measures Group and scottish Coal measures Group 

Cochno lavas Cochno lava member, Clyde plateau volcanic Formation 

Cockermouth lavas Cockermouth volcanic Formation 

‘Cornstone-bearing beds’ lindsayston Burn member, Ballagan Formation 

Cornstone Beds Kinneswood Formation 

Corrie lavas Corrie lava member, Clyde plateau volcanic Formation 

Cottonshope lavas Cottonshope volcanic Formation 

Craigdouffie lavas Craigdouffie lava member, Clyde plateau volcanic Formation 

Craigentimpin lavas Craigentimpin lava member, Clyde plateau volcanic Formation 

Craigmaddie sandstone Formation Craigmaddie muir sandstone member, lawmuir Formation 

Craigmaddie sandstones Craigmaddie muir sandstone member, lawmuir Formation 

Crichope sandstone member Townburn sandstone member, passage Group 

darvel lavas darvel lava member, Clyde plateau volcanic Formation 

denny muir lavas denny muir lava member, Clyde plateau volcanic Formation 

downie’s loop sandstone Formation Clyde sandstone Formation, inverclyde Group 

drumnessie lavas drumnessie lava member, Clyde plateau volcanic Formation 

dryburn limestone Great limestone member, Alston Formation 

dug Head sandstone member doughend sandstone member, Kinnesswood Formation 

dumdruff Hill lavas dumdruff Hill lava member, Clyde plateau volcanic Formation 

eaglesham lavas eaglesham lava member, Clyde plateau volcanic Formation 

east linton member east linton lava member, Garleton Hills volcanic Formation 

eight yard limestone Four Fathom limestone member, Alston Formation 

Faughlin lavas Faughlin lava member, Clyde plateau volcanic Formation 

Fereneze lavas Fereneze lava member, Clyde plateau volcanic Formation 

Fin Glen lavas Fin Glen lava member, Clyde plateau volcanic Formation 

Fintry Hills Group Fintry Hills lava member, Clyde plateau volcanic Formation 

Five yard limestone Five yard limestone member, Alston Formation 

Flow moss lavas lower and upper Flow moss lava members, Clyde plateau 

volcanic Formation 

Four Fathom limestone Four Fathom limestone member, Alston Formation 

Gargunnock Hills Group Gargunnock Hills lava member, Clyde plateau volcanic 

Formation 

Garvald lavas Garvald lava member, Clyde plateau volcanic Formation 

Gillfoot sandstone Formation Gillfoot sandstone member, Fell sandstone Formation 

Gleaston Formation Alston Formation 

Glen park volcanic detrital member Glenburn volcaniclastic member, Clyde plateau volcanic 

Formation 

Gleniffer lavas Gleniffer lava member, Clyde plateau volcanic Formation 

Grassington Grit Formation pendleton Formation 

Great limestone Great limestone member, Alston Formation 

Greeto lavas Greeto lava member, Clyde plateau volcanic Formation 

Hailes member Hailes lava member, Garleton Hills volcanic Formation 

Harelaw lavas Harelaw lava member, Clyde plateau volcanic Formation 

Harelawhill limestone eelwell limestone member, Alston Formation 

Hensingham Group stainmore Formation 

Holehead lavas Holehead lava member, Clyde plateau volcanic Formation 

Jew limestone Jew limestone member, Alston Formation 

Kelso lavas Kelso volcanic Formation 

Kelso Traps Kelso volcanic Formation 

Kettlewell Crag member park limestone Formation 



162

Kilbarchan lavas Kilbarchan lava member, Clyde plateau volcanic Formation 

Kilbirnie mudstone Formation Kilbirnie mudstone member, limestone Coal Formation 

Kilnsey limestone member scaleber Quarry limestone member, Kilnsey Formation 

Kilnsey limestone-with-mudstone member scaleber Force limestone member, Kilnsey Formation 

Kirkbean Cementstone Formation Kirkbean Cementstone member, Ballagan Formation 

Knowehead lavas Knowehead lava member, Clyde plateau volcanic Formation 

ladies wood limestone dun limestone member, Tyne limestone Formation 

laird’s Hill lavas laird’s Hill lava member, Clyde plateau volcanic Formation 

laird’s loup lavas laird’s loup lava member, Clyde plateau volcanic Formation 

lamberton limestone dun limestone member, Tyne limestone Formation 

langhill lavas langhill lava member, Clyde plateau volcanic Formation 

largs lavas largs lava member, Clyde plateau volcanic Formation 

lees Hill Group lees Hill lava member, Clyde plateau volcanic Formation 

leswalt Formation scottish Coal measures Group 

limestone Coal Group limestone Coal Formation 

loup of Fintry lavas loup of Fintry lava member, Clyde plateau volcanic Formation 

low dean limestone Four Fathom limestone member, Alston Formation 

lower Border Group Ballagan Formation, inverclyde Group and lyne Formation, 

Border Group 

lower Coal measures pennine lower Coal measures Formation and scottish lower Coal 

measures Formation 

lower lecket Hill lavas lower lecket Hill lava member, Clyde plateau volcanic 

Formation 

lower liddesdale Group Tyne limestone Formation 

lower limestone Group Tyne limestone Formation and Alston Formation 

lower limestone Group lower limestone Formation, Clackmannan Group 

lower North Campsie lavas Campsie lava member, Clyde plateau volcanic Formation 

lower south Campsie lavas Campsie lava member, Clyde plateau volcanic Formation 

low Furness Basal Beds marsett Formation 

low Furness Basal Formation marsett Formation 

lynebank Beds lynebank member, lyne Formation 

main Algal limestone Beds main Algal member, lyne Formation 

main limestone Great limestone member, Alston Formation 

main limestone Group Great scar limestone Group 

‘marginal reef limestones’ Cracoe limestone Formation 

marshall moor lavas marshall moor lava member, Clyde plateau volcanic Formation 

Michelinia grandis beds Breakyneck scar limestone Formation 

middle Border Group Fell sandstone Formation 

middle Coal measures pennine middle Coal measures Formation and scottish middle 

Coal measures Formation 

middle Grit Group marsden Formation 

middle limestone Formation Alston Formation 

middle limestone Group Alston Formation 

millstone Grit series Clackmannan Group (undivided) 

misty law Trachytic Centre misty law Trachitic member, Clyde plateau volcanic Formation 

moyne moor lavas moyne moor lava member, Clyde plateau volcanic Formation 

mugdock lavas mugdock lava member, Clyde plateau volcanic Formation 

Neilston lavas Neilston lava member, Clyde plateau volcanic Formation 

Noddsdale volcaniclastic Beds Noddsdale volcaniclastic member, Clyde plateau volcanic Formation 

North Berwick member North Berwick pyroclastic member, Garleton Hills volcanic Formation 

163 



orroland Formation orroland member, Ballagan Formation 

orton Formation Frizzington limestone Formation 

orton Group Frizzington limestone Formation 

overton lavas overton lava member, Clyde plateau volcanic Formation 

overtoun sandstone Formation overtoun sandstone member, Clyde sandstone Formation 

passage Group passage Formation 

passage Group (undivided) Townburn sandstone member, passage Group 

penny Farm Gill dolomite Formation penny Farm Gill Formation 

pinskey Gill Beds pinskey Gill Formation 

powillimount Beds powillimount sandstone member, Fell sandstone Formation 

powillimount sandstone Formation powillimount sandstone member, Fell sandstone Formation 

Rascarrel Formation Rascarrel member, Fell sandstone Formation 

‘Red measures’ warwickshire Group 

Roman Fell Beds marsett Formation 

Roman Fell sandstones marsett Formation 

Roman Fell shales marsett Formation 

sandbanks limestone Four Fathom limestone member, Alston Group 

sandwick member sandwick (isle of man) member, derbyhaven Formation 

saughen Braes lavas saughen Braes lava member, Clyde plateau volcanic Formation 

scarlett Beds scarlett point member, Bowland shale Formation 

scarlett volcanic Formation scarlett volcanic member, Bowland shale Formation 

scarlett volcanic series scarlett volcanic member, Bowland shale Formation 

second limestone Four Fathom limestone member, Alston Formation 

shap limestone shap village limestone Formation 

shelloch Burn Group shelloch Burn lava member, Clyde plateau volcanic Formation 

sixth shale member sixth limestone, eskett limestone Formation 

skiddaw Group skiddaw lava member, Clyde plateau volcanic Formation 

slackgun interbasaltic Beds slackgun volcaniclastic member, Clyde plateau volcanic 

Formation 

southerness Beds southerness limestone member, lyne Formation 

southerness limestone Formation southerness limestone member, lyne Formation 

spout of Ballochleam Group spout of Ballochleam lava member, Clyde plateau volcanic 

Formation 

strandhall Beds scarlett point member, Bowland shale Formation 

strathgryfe lavas strathgryfe lava member, Clyde plateau volcanic Formation 

stronend interbasaltic Beds stronend volcaniclastic member, Clyde plateau volcanic Formation 

Tambowie lavas Tambowie lava member, Clyde plateau volcanic Formation 

Tappetknowe lavas Tappetknowe lava member, Clyde plateau volcanic Formation 

Tarn sike limestones Breakyneck scar limestone Formation 

Third limestone Three yard limestone member, Alston Formation 

Thirlstane sandstone powillimount sandstone member, Fell sandstone Formation 

Thorney Force sandstone wintertarn sandstone member, Alston Formation 

Touch House Group Touch House lava member, Clyde plateau volcanic Formation 

Troon volcanic Formation Troon volcanic member, passage Formation 

Tyne Bottom limestone Tynebottom limestone member, Alston Formation 

undersett limestone Four Fathom limestone member, Alston Formation 

upper Border Group Tyne limestone Formation 

upper Bowland shale Formation Bowland shale Formation 

upper Coal measures Formation pennine upper Coal measures and scottish upper Coal measures 

Formation 



164

upper lecket Hill lavas upper lecket Hill lava member, Clyde plateau volcanic Formation 

upper liddesdale Group Alston Formation 

upper limestone Group upper limestone Formation 

upper Michelinia Beds skillicore member, derbyhaven Formation 

upper North Campsie lavas Campsie lava member, Clyde plateau volcanic Formation 

upper oil shale Group Hopetoun member, west lothian oil-shale Formation 

upper south Campsie lavas Campsie lava member, Clyde plateau volcanic Formation 

wall Hill sandstone Formation wall Hill member, Ballagan Formation 

wall Hill sandstone Group wall Hill member, Ballagan Formation 

wensleydale Group yoredale Group 

165

A lithostratigraphical framework for the Carboniferous successions of

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